The 6 September 1997 (Mw4.5) Coatzacoalcos-Minatitlán, Veracruz, Mexico earthquake: implications for tectonics and seismic hazard of the region

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(b) Aspect of the deposit. The insert shows some of the fragments collected at this site.(c) Granulometry of the matrix of the deposit." ] ] ] "autores" => array:1 [ 0 => array:2 [ "autoresLista" => "Araceli Zamora-Camacho, Juan Manuel Espíndola, Peter Schaaf, Angel Ramírez, María de Lourdes Godínez Calderón" "autores" => array:5 [ 0 => array:2 [ "nombre" => "Araceli" "apellidos" => "Zamora-Camacho" ] 1 => array:2 [ "nombre" => "Juan Manuel" "apellidos" => "Espíndola" ] 2 => array:2 [ "nombre" => "Peter" "apellidos" => "Schaaf" ] 3 => array:2 [ "nombre" => "Angel" "apellidos" => "Ramírez" ] 4 => array:2 [ "nombre" => "María de Lourdes Godínez" "apellidos" => "Calderón" ] ] ] ] ] "idiomaDefecto" => "en" "EPUB" => "https://multimedia.elsevier.es/PublicationsMultimediaV1/item/epub/S0016716915000227?idApp=UINPBA00004N" "url" => "/00167169/0000005400000003/v2_201509120041/S0016716915000227/v2_201509120041/en/main.assets" ] "en" => array:19 [ "idiomaDefecto" => true "titulo" => "The 6 September 1997 (Mw4.5) Coatzacoalcos-Minatitlán, Veracruz, Mexico earthquake: implications for tectonics and seismic hazard of the region" "tieneTextoCompleto" => true "paginas" => array:1 [ 0 => array:2 [ "paginaInicial" => "289" "paginaFinal" => "298" ] ] "autores" => array:1 [ 0 => array:4 [ "autoresLista" => "Shri Krishna Singh, José Francisco Pacheco, Xyoli Pérez-Campos, Mario Ordaz, Eduardo Reinoso" "autores" => array:5 [ 0 => array:4 [ "nombre" => "Shri Krishna" "apellidos" => "Singh" "email" => array:1 [ 0 => "krishnamex@yahoo.com" ] "referencia" => array:2 [ 0 => array:2 [ "etiqueta" => "a" "identificador" => "aff0005" ] 1 => array:2 [ "etiqueta" => "*" "identificador" => "cor0005" ] ] ] 1 => array:3 [ "nombre" => "José Francisco" "apellidos" => "Pacheco" "referencia" => array:1 [ 0 => array:2 [ "etiqueta" => "b" "identificador" => "aff0010" ] ] ] 2 => array:3 [ "nombre" => "Xyoli" "apellidos" => "Pérez-Campos" "referencia" => array:1 [ 0 => array:2 [ "etiqueta" => "a" "identificador" => "aff0005" ] ] ] 3 => array:3 [ "nombre" => "Mario" "apellidos" => "Ordaz" "referencia" => array:1 [ 0 => array:2 [ "etiqueta" => "c" "identificador" => "aff0015" ] ] ] 4 => array:3 [ "nombre" => "Eduardo" "apellidos" => "Reinoso" "referencia" => array:1 [ 0 => array:2 [ "etiqueta" => "c" "identificador" => "aff0015" ] ] ] ] "afiliaciones" => array:3 [ 0 => array:3 [ "entidad" => "Instituto de Geofísica Universidad Nacional Autónoma de México Ciudad Universitaria Delegación Coyoacán, 04510, México D.F., México" "etiqueta" => "a" "identificador" => "aff0005" ] 1 => array:3 [ "entidad" => "Observatorio Vulcanológico y Sismológico de Costa Rica Universidad Nacional" "etiqueta" => "b" "identificador" => "aff0010" ] 2 => array:3 [ "entidad" => "Instituto de Ingeniería Universidad Nacional Autónoma de México Ciudad Universitaria Delegación Coyoacán, 04510, México D.F., México" "etiqueta" => "c" "identificador" => "aff0015" ] ] "correspondencia" => array:1 [ 0 => array:3 [ "identificador" => "cor0005" "etiqueta" => "⁎" "correspondencia" => "Corresponding author." ] ] ] ] "resumenGrafico" => array:2 [ "original" => 0 "multimedia" => array:7 [ "identificador" => "fig0010" "etiqueta" => "Figure 2" "tipo" => "MULTIMEDIAFIGURA" "mostrarFloat" => true "mostrarDisplay" => false "figura" => array:1 [ 0 => array:4 [ "imagen" => "gr2.jpeg" "Alto" => 573 "Ancho" => 1872 "Tamanyo" => 132680 ] ] "descripcion" => array:1 [ "en" => "Seismograms at station TUIG during the 6 September 1997 earthquake. (a) Acceleration, (b) velocity, and (c) displacement. The traces in (b) and (c) have been obtained by integration of the accelerograms shown in (a)." ] ] ] "textoCompleto" => "IntroductionA detailed analysis of the Mw4.5 earthquake of 6 September 1997, which occurred near Coatzacoalcos-Minatitlán, Veracruz, is of interest for three reasons. First, the surface and the near-surface information from volcanic alignments, borehole elongations, and unpublished PEMEX seismic sections points to active normal-faulting in the region (<a class="elsevierStyleCrossRef" href="#bib0130">Suter, 1991</a>). The focal mechanism of an earthquake which occurred nearby on 26 August 1959 (Mw6.4), however, shows thrust faulting at a depth of about 26km (<a class="elsevierStyleCrossRefs" href="#bib0135">Wickens and Hodgson, 1967; Suárez, 2000</a>; see <a class="elsevierStyleCrossRef" href="#fig0005">Figure 1</a>). It is, therefore, of interest to know whether the 1997 earthquake confirms such a change in the stress regime (permutation of the least and maximum principal stresses) with depth in the region. In most regions, the stress regime at relatively shallow depth agrees with that at mid-crustal depth. There are some exceptions (see, e.g., Zoback and Zoback, 1991) and one such exception appears to be the coastal plain of the Gulf of Mexico (<a class="elsevierStyleCrossRef" href="#bib0050">Frohlich, 1982</a>; Zoback and Zoback, 1991; <a class="elsevierStyleCrossRef" href="#bib0130">Suter, 1991</a>). Another classical example is the decoupling of the stress field across the basal detachment of the Jura fold-thrust belt; the near-surface stress field is different from that in the basement (<a class="elsevierStyleCrossRef" href="#bib0010">Becker et al., 1987</a>).<elsevierMultimedia ident="fig0005"></elsevierMultimedia>Second, the earthquake of 26 August 1959 caused serious damage to the towns of Jáltipan, Coatzacoalcos, and Minatitlán (<a class="elsevierStyleCrossRefs" href="#bib0035">Figueroa, 1964; Rosenblueth, 1964</a>; Resén-diz, 1964). The latter two towns have beco-me important industrial centers related to the intense activity of PEMEX, the national petroleum company, and population has grown by 22% in the last 10 years to reach more than half million people (<a class="elsevierStyleCrossRef" href="#bib0055">INEGI, 2010</a>). For this reason, it is important to estimate ground motions that may be expected in these towns if an earthquake, such as that of 1959, were to recur in the region. We may use the records of the 1997 earthquakes obtained at the near-source broadband station of TUIG as empirical Green's function to simulate the corresponding motions from an Mw6.4 event. Although the station is about 25km SE of Coatzacoalcos-Minatitlán, the geology of these sites is roughly similar; to a first approximation, the results for the TUIG site may be valid for the entire region in case of an earthquake at about the same focal distance from TUIG as the event of 1997.Finally, a study of the 1997 earthquake (and other events in and along the Gulf of Mexico) has an important bearing on the seismic safety of the Laguna Verde nuclear power plant (<a class="elsevierStyleCrossRef" href="#fig0005">Figure 1</a>) as well as the hydrocarbon exploration and production facilities in this region.Data and analysisThe 1997 earthquake was recorded by the local broadband station TUIG (S-P time = 5 s) and by seven other broadband stations of the National Seismological Service (SSN), which were located at epicentral distances greater than 260km. The reported coda-wave magnitude, Mc, is 4.3. The epicenter of the event, given by the SSN, is 18.146 °N and 94.499 °W. However, its focal depth could not be constrained. The epicenter and focal depth reported by the National Earthquake Information Center (NEIC), U.S. Geological Survey, are 18.017 °N and 94.396 °W and 33km, respectively. This depth was fixed by NEIC in the location of the earthquake.For moderate Mexican earthquakes it is now possible to obtain a regional centroid moment tensor (CMT) solution using relatively long-period regional waveforms (see, e.g., <a class="elsevierStyleCrossRef" href="#bib0090">Pacheco and Singh, 1998</a>). Unfortunately, the seismograms of the 1997 earthquake show little energy at periods greater than 10 s because of its relatively small magnitude. At shorter periods, a detailed three-dimensional crustal structure is needed to model the observed seismograms but is currently lacking for the region. For these reasons it was not possible to obtain a CMT solution by inverting the regional waveforms.A single, near-source, three-component broadband recording can be used to find a reliable location, origin time, and focal mechanism of an earthquake, provided that a rough initial guess of the mechanism is available from other data (see, e.g., <a class="elsevierStyleCrossRefs" href="#bib0060">Kanamori et al., 1990; Singh et al., 1997, 2000a</a>). The calculation of the location and origin time requires clear first arrivals on each of the three components of the ground motion as well as the knowledge of the local crustal structure. <a class="elsevierStyleCrossRef" href="#fig0010">Figure 2</a> shows acceleration, velocity and displacement traces at TUIG during the 6 September 1997 earthquake. <a class="elsevierStyleCrossRef" href="#fig0015">Figure 3</a> illustrates the initial part of the three components of displacement at TUIG. Note that the horizontal components have been amplified by a factor of 20. The incidence of initial P-wave at the station is nearly vertical. Nevertheless, it can be seen that the station is located in the NW quadrant with respect to the source. The amplitude towards west at time 0.172 s is 3.5 times that towards north. It follows that the station azimuth, φs, is 286°. Before proceeding further with the analysis of the source parameters of this earthquake, we summarize our knowledge of the local crustal structure.<elsevierMultimedia ident="fig0010"></elsevierMultimedia><elsevierMultimedia ident="fig0015"></elsevierMultimedia>Crustal structure of the regionThe P-wave speed, a, in the shallow crust south and near Coatzacoalcos is available from exploration seismology carried out by PEMEX (A. Camargo, personal communication, 1997). The crust consists of a 1.8km thick layer with a = 2.5km/s, overlying a layer of a = 4.25km/s. The thickness of the second layer exceeds 3.4km, the maximum depth reached by boreholes. Based on receiver function analysis, <a class="elsevierStyleCrossRef" href="#bib0025">Cruz-Atienza (2000)</a> reports sediment thickness of 16km below TUIG. N. Shapiro (unpublished report) inverted group velocity dispersion curve corresponding to the region between the City of Oaxaca and TUIG. In the inversion, Shapiro fixed the thickness of the first layer and a values of the first and the second layers to the values given by PEMEX. The shear-wave speeds, b, of the first and second layers were taken as 1.4km/s and 2.4km/s, respectively. The crustal model adopted from the results of <a class="elsevierStyleCrossRef" href="#bib0025">Cruz-Atienza (2000)</a> and N. Shapiro, and used by us in generating synthetic seismograms, is given in <a class="elsevierStyleCrossRef" href="#tbl0005">Table 1</a>. In this table, the densities and the quality factors, Q, of the layers have been taken arbitrarily; the results are not very sensitive to their choices.<elsevierMultimedia ident="tbl0005"></elsevierMultimedia>Source parameters of the earthquakeBased on the crustal model in <a class="elsevierStyleCrossRef" href="#tbl0005">Table 1</a> and the (S-P) time of 5 s at station TUIG, the maximum depth of the earthquake, Hmax, assuming the station to be located directly above the focus, is 30.9km. If the thickness of the second layer in <a class="elsevierStyleCrossRef" href="#tbl0005">Table 1</a> is taken as 10km, then Hmax becomes 34.8km. Near-vertical incidence at TUIG may be a consequence of both small epicentral distance as compared to the source depth, and refraction of waves caused by progressively lower seismic speeds near the surface.<a class="elsevierStyleCrossRef" href="#fig0020">Figure 4</a>, top, shows P-wave first-motion polarities at those Mexican and teleseismic stations where they could be read unequivocally. These data suggest a thrust-faulting earthquake with possible strike-slip component. The first motion polarities provide some constrains on the azimuth (140° ≤ f ≤ 190°) and the dip (45° ≤ δ ≤ 85°) of one of the nodal planes but the rake, l, of this plane can vary between 35° and 120°. To determine the focal mechanism, we performed a waveform inversion of the displacement traces recorded at TUIG. For the inversion the event was approximated by a point-source shear dislocation. Synthetic seismograms include near- and intermediate-field contributions (<a class="elsevierStyleCrossRef" href="#bib0115">Singh et al., 2000a</a>). The effect of the free surface is approximately taken into account by multiplying the infinite-space synthetics by two. This approximation is acceptable if the epicentral distance, Δ, is smaller than the depth, H. We took the sta-tion azimuth, fs, as 286°, the take-off angle from the source, ih, as 170°, and the angle of incidence at the surface, iO, as 5° from the vertical. Based on the observed P-pulse on the Z-component (<a class="elsevierStyleCrossRef" href="#fig0010">Figure 2</a>c), we chose a triangular source with duration, t, of 0.38 s. We varied the azimuth, dip, and rake within the ranges mentioned above. No contradiction of the first motion polarities was allowed. The two nodal planes obtained from the inversion are: f = 150°; d = 70°; l = 90° and f = 330°; d = 20°; l = 90°. The observed and synthetic seismograms are shown in the bottom left of <a class="elsevierStyleCrossRef" href="#fig0020">Figure 4</a>.<elsevierMultimedia ident="fig0020"></elsevierMultimedia>We generated synthetic seismograms corresponding to this focal mechanism and the crustal model given in <a class="elsevierStyleCrossRef" href="#tbl0005">Table 1</a>. <a class="elsevierStyleCrossRef" href="#bib0020">Bouchon's (1982)</a> discrete wave number algorithm was used in the computation. We again took fs = 286° and t = 0.38 s. A good fit between observed and synthetic seismograms at TUIG was found for an epicentral distance of 7km, a depth of 30km, and M0 = 6.0x1015 N-m (Mw4.5) (<a class="elsevierStyleCrossRef" href="#fig0020">Figure 4</a>, bottom right). <a class="elsevierStyleCrossRef" href="#tbl0010">Table 2</a> summarizes the relevant source parameters of this earthquake.<elsevierMultimedia ident="tbl0010"></elsevierMultimedia>Stress regime of the Gulf coast region of Coatzacoalcos-MinatitlánIn spite of some uncertainty in its focal mechanism, there is no doubt that the 1997 earthquake was a thrust event with, probably, some strike-slip component. Its source was below the Comalcalco basin at a depth of about 30km. As mentioned earlier, the surface and the near-surface information from volcanic alignments, borehole elongations, and unpublished PEMEX seismic sections in the Gulf coast basin region of Coatzacoalcos-Minatitlán suggest active normal-faulting in the upper few kilometers (<a class="elsevierStyleCrossRef" href="#bib0130">Suter, 1991</a>). Thus, there is a change of stress regime from extension in the sediments of the upper crust to shortening in the mid- and lower crust indicated by focal mechanisms (<a class="elsevierStyleCrossRef" href="#fig0005">Figure 1</a>). A similar change of stress regime with depth is reported in the central Gulf of Mexico by <a class="elsevierStyleCrossRef" href="#bib0050">Frohlich (1982)</a> from an analysis of an earthquake in 1978 at the edge of the Mississippi Fan at a depth of 15km (<a class="elsevierStyleCrossRef" href="#fig0005">Figure 1</a>). Other cases of stress change below sedimentary basins are discussed in Zoback and Zoback (1991). Extension in upper part of crust is probably controlled by gravitational load and major topographic gradient, at least in the adjacent Veracruz basin.<a class="elsevierStyleCrossRef" href="#tbl0010">Table 2</a> lists seven intraplate earthquakes located in and near the Gulf of Mexico with known focal mechanisms. It includes the earthquakes of 1978 and 1997. The locations of these events and their focal mechanisms are illustrated in <a class="elsevierStyleCrossRef" href="#fig0005">Figure 1</a>. For the earthquakes of 2007 and 2009, more than one solution is available (<a class="elsevierStyleCrossRef" href="#tbl0010">Table 2</a>). For these two earthquakes, the Global CMT location and focal mechanism is shown. As most intraplate regions, the Gulf is characterized by thrust-type stress regime (<a class="elsevierStyleCrossRef" href="#bib0140">Zoback et al., 1989</a>). The orientations of the P-axes of the 1959, 1967, 2006, 2007 and 2009 earthquakes range between N30°E and N65°E. These are consistent with reported offshore stress orientations near the same region, inferred from breakouts (<a class="elsevierStyleCrossRefs" href="#bib0145">Zoback et al., 1990; Suter, 1991</a>; World Stress Map, <a href="http://dc-app3-14.gfz-potsdam.de/">http://dc-app3-14.gfz-potsdam.de/</a>, 12 May 2015). These orientations fall between the directions of: (1) the relative convergence of the Cocos and North American plates and (2) the absolute motion of the North American plate. Perhaps both the relative convergence and the absolute motion are responsible for the observed P-axis, with the former playing a more dominant role for events in and near the SSW Gulf due to their relative proximity to the middle America subduction zone (earthquakes of 1959, 1967, 1997, and 2009) and the latter being dominant for the events of 2006 and 2007 which are relatively far from the plate boundary. For the 2006 earthquake, sliding of Sigsbee salt and landslide have also been suggested as possible causes (<a class="elsevierStyleCrossRefs" href="#bib0080">Nettles, 2007; Franco et al., 2013</a>).<a class="elsevierStyleCrossRef" href="#bib0030">Dewey and Suárez (1991)</a> and <a class="elsevierStyleCrossRef" href="#bib0125">Suárez (2000)</a> suggest that the intraplate, mid- and lower-crust compression below the Comalcalco basin, as revealed by the 1959 and 1967 earthquakes, may be a consequence of strong coupling along the plate interface where the Tehuantepec ridge subducts below Mexico. This may also be true for the 1997 and 2009 earthquakes. If so, then, unlike subduction of many other ridges (<a class="elsevierStyleCrossRef" href="#bib0070">Kelleher and McCann, 1976</a>), the Tehuantepec ridge does not subduct aseismically. Since there is no clear evidence for major/great earthquakes in the Tehuantepec region during the last two centuries (see, e.g., <a class="elsevierStyleCrossRef" href="#bib0105">Singh et al., 1981</a>), it could mean that the recurrence period of such events in this segment is much greater than in other segments along the Mexican subduction zones where it is ∼ 30 to 75 years (<a class="elsevierStyleCrossRefs" href="#bib0105">Singh et al., 1981; Astiz and Kanamori, 1984</a>).As for the 1978 Mississippi Fan earthquake (<a class="elsevierStyleCrossRef" href="#fig0005">Figure 1</a>), the P-axis does not follow the trend of the other events. The compressional nature of this earthquake was interpreted by <a class="elsevierStyleCrossRef" href="#bib0050">Frohlich (1982)</a> as a consequence of downwarping of the lithosphere due to sediment accumulation.Expected ground motions in the Coatzacoalcos-Minatitlán region from a postulated Mw6.4 earthquakeThe earthquake of 1959 destroyed a majority of the dwellings in the town of Jáltipan (<a class="elsevierStyleCrossRef" href="#bib0100">Rosenblueth, 1964</a>). Many buildings suffered structural or foundation failures in Coatzacoalcos and Minatitlán (<a class="elsevierStyleCrossRefs" href="#bib0075">Marsal, 1961; Reséndiz, 1964</a>). The land near the port of Coatzacoalcos subsided. Some of the effects of the earthquake were attributed to partial liquefaction of sand and silt (<a class="elsevierStyleCrossRef" href="#bib0075">Marsal, 1961</a>). Modified Mercalli (MM) intensities in these towns during this earthquake were VIII (<a class="elsevierStyleCrossRef" href="#bib0035">Figueroa, 1964</a>). The 1959 earthquake was not an isolated event. The epicenter of the earthquake of 11 January, 1946 was apparently close to that of 1959 (<a class="elsevierStyleCrossRef" href="#bib0035">Figueroa, 1964</a>). The earthquake of 1946 was assigned a magnitude of 6.0 (<a class="elsevierStyleCrossRef" href="#bib0040">Figueroa, 1970</a>) and a MM intensity of VII in Coatzacoalcos (<a class="elsevierStyleCrossRef" href="#bib0035">Figueroa, 1964</a>). The towns of Coatzacoalcos and Minatitlán are now important centers of national petroleum activity. Thus, it is of significant earthquake engineering interest to estimate the ground motions in these towns during a future local Mw6.4 earthquake.To estimate the ground motions from an Mw6.4 earthquake, we used the recording of 1997 earthquake as an empirical Green's function (EGF) and a method proposed by <a class="elsevierStyleCrossRef" href="#bib0085">Ordaz et al. (1995)</a> which is based on adding N scaled EGF records, each differed in time by a random delay. The probability distribution of the delays is such that, on average, the simulations follow an w2-spectral scaling at all frequencies. The method requires specification of the seismic moment, M0, and the stress drop, Ds, of both the EGF and the target earthquake. In our case, M0 of the EGF is 6x1015 N-m and that of the target event is 5x1018 N-m (Mw6.4). A rough estimate of the static stress drop of the EGF can be obtained from the following considerations. For a circular rupture, the radius, a, of the fault can be estimated by (<a class="elsevierStyleCrossRef" href="#bib0015">Boatwright, 1980</a>):<elsevierMultimedia ident="eq0005"></elsevierMultimedia>where t1/2 is the rise time of the far-field pulse, v is the rupture speed, c is the wave speed, and q is the take-off angle measured from fault normal. For this event, t1/2 is about 0.19 s (<a class="elsevierStyleCrossRef" href="#tbl0010">Table 2</a>, <a class="elsevierStyleCrossRef" href="#fig0010">Figure 2</a>c). For S wave, c = b, which we take as 3.75km/s (<a class="elsevierStyleCrossRef" href="#tbl0005">Table 1</a>). Assuming f = 330°; d = 20°; l = 90° as the fault plane and ih =170°, q is ∼10°. For v = 0.9b, we obtain a fault radius a = 0.76km (equation 1). For a circular fault, Ds is related to M0 and a by (<a class="elsevierStyleCrossRef" href="#bib0065">Keilis-Borok, 1959</a>):<elsevierMultimedia ident="eq0010"></elsevierMultimedia>which gives Ds of ∼ 6MPa for the EGF. In the simulations, we take Ds of the EGF and the target event to be either 6MPa or 12MPa. Typical simulated acceleration, velocity, and displacement traces, corresponding to Ds = 6MPa for both events, are illustrated in <a class="elsevierStyleCrossRef" href="#fig0025">Figure 5</a>. In the figure, we compare deterministic, synthetic displacement seismograms with ones obtained by random summation of EGF. The synthetics were generated at TUIG for an event with M0 = 5x1018 N-m (Mw6.4), located at the same focus as the 1997 earthquake, and having the same focal mechanism. The duration of the source time function, t, of Mexican earthquakes is related to their seismic moment by<elsevierMultimedia ident="eq0015"></elsevierMultimedia><elsevierMultimedia ident="fig0025"></elsevierMultimedia>(<a class="elsevierStyleCrossRef" href="#bib0120">Singh et al., 2000b</a>). Thus, the estimated t for the target event is 4.2 s. A point source with a triangular source-time function of 4.2 s duration and the crustal structure given in <a class="elsevierStyleCrossRef" href="#tbl0005">Table 1</a> were taken for the computation. The PGD values are within a factor of two of each other. Both calculations show important near-field contribution (the ramp-like wave between P and S wave).Results of simulation for various combinations of Ds are summarized in <a class="elsevierStyleCrossRef" href="#tbl0015">Table 3</a>. The expected horizontal PGA, PGV, and PGD range between 120 and 260gal, 12 and 28cm/s, and 6 and 11cm, respectively.<elsevierMultimedia ident="tbl0015"></elsevierMultimedia>Although the ground motions estimated by random summation of the EGF are reasonable, there are several factors which introduce uncertainties in these results. The stress drop of the EGF event is uncertain and that of the target earthquake is assumed. The directivity of the source may give rise to greater or smaller ground motions than those computed by our method. Finally, a single EGF may not be adequate to sample the entire fault plane of an Mw6.4.We emphasize that this synthesis of the ground motion is based on the assumption of linear elastic response of the sediments. Almost certainly the shallow sediments of the Gulf basin will behave nonlinearly under such excitation, as was the case during the 1959 earthquake. In view of the uncertainties, the observed ground motions may easily differ by a factor of 2 or 3 from the expected ones. This however is usually the case in ground motion predictions.ConclusionsOur analysis shows that the 6 September 1997 earthquake (H = 30km; Mw4.5), like the nearby earthquake of 26 August 1957 (H = 21km; Mw6.4), was a thrust event. The event confirms a previous conclusion that while the upper sediments of the Gulf coast basins are in an extensional (normal fault-type) stress regime, the mid- and lower crust is in a shortening (thrust fault-type) stress regime (<a class="elsevierStyleCrossRefs" href="#bib0030">Dewey and Suárez, 1991; Suter, 1991</a>), which implies a permutation between the vertical and maximum horizontal principal stresses. Upper crust is under extension probably because of gravitational loads and high topographic gradient; the stress field of middle to lower crust may be controlled by far-field loads at convergent plate margin and/or absolute plate motion.Our estimation of ground motion in the epicentral region of Comalcalco basin due to a postulated Mw6.4 earthquake indicates that peak acceleration, velocity, and displacement (assuming linear behavior of the sediments) may be in the range of 120-260gal, 12-28cm/s, and 6-11cm, respectively. These, then, are also our estimations of the ground motions during the 1959, Mw6.4, earthquake. These estimations were obtained using 6 September 1997 event as an empirical Green's function under various simplifying, though reasonable, assumptions. They are valid for sites with local geology similar to that of station TUIG. The estimation of ground motions at other nearby sites, such as Minatitlán, may be calculated if their site responses are known. Subjected to such ground motions the sediments of the Gulf Coast are likely to behave nonlinearly and may liquefy, as was the case during the 1959 earthquake." "textoCompletoSecciones" => array:1 [ "secciones" => array:14 [ 0 => array:3 [ "identificador" => "xres551708" "titulo" => "Resumen" "secciones" => array:1 [ 0 => array:1 [ "identificador" => "abst0005" ] ] ] 1 => array:2 [ "identificador" => "xpalclavsec569122" "titulo" => "Palabras clave" ] 2 => array:3 [ "identificador" => "xres551709" "titulo" => "Abstract" "secciones" => array:1 [ 0 => array:1 [ "identificador" => "abst0010" ] ] ] 3 => array:2 [ "identificador" => "xpalclavsec569123" "titulo" => "Keywords" ] 4 => array:2 [ "identificador" => "sec0005" "titulo" => "Introduction" ] 5 => array:2 [ "identificador" => "sec0010" "titulo" => "Data and analysis" ] 6 => array:2 [ "identificador" => "sec0015" "titulo" => "Crustal structure of the region" ] 7 => array:2 [ "identificador" => "sec0020" "titulo" => "Source parameters of the earthquake" ] 8 => array:2 [ "identificador" => "sec0025" "titulo" => "Stress regime of the Gulf coast region of Coatzacoalcos-Minatitlán" ] 9 => array:2 [ "identificador" => "sec0030" "titulo" => "Expected ground motions in the Coatzacoalcos-Minatitlán region from a postulated M6.4 earthquake" ] 10 => array:2 [ "identificador" => "sec0035" "titulo" => "Conclusions" ] 11 => array:2 [ "identificador" => "xack186047" "titulo" => "Acknowledgments" ] 12 => array:1 [ "titulo" => "Further reading" ] 13 => array:1 [ "titulo" => "References" ] ] ] "pdfFichero" => "main.pdf" "tienePdf" => true "fechaRecibido" => "2014-05-20" "fechaAceptado" => "2014-08-12" "PalabrasClave" => array:2 [ "es" => array:1 [ 0 => array:4 [ "clase" => "keyword" "titulo" => "Palabras clave" "identificador" => "xpalclavsec569122" "palabras" => array:4 [ 0 => "Sismo de Jáltipan" 1 => "movimientos fuertes" 2 => "tectónica del Golfo de México" 3 => "peligro sísmico del Golfo de México." ] ] ] "en" => array:1 [ 0 => array:4 [ "clase" => "keyword" "titulo" => "Keywords" "identificador" => "xpalclavsec569123" "palabras" => array:4 [ 0 => "Jáltipan earthquake" 1 => "strong motion" 2 => "tectonic of the Gulf of México" 3 => "seismic hazards of the Gulf of México" ] ] ] ] "tieneResumen" => true "resumen" => array:2 [ "es" => array:2 [ "titulo" => "Resumen" "resumen" => "Analizamos el sismo del 6 de septiembre de 1997 (Mw4.5), que se produjo a unos 25km al SE de Coatzacoalcos, Veracruz. El sismo fue registrado por la estación local TUIG de banda ancha de (tiempo S-P = 5 s). Las polaridades de la onda P a distancias regionales y telesísmicas, y el modelado de las formas de onda de desplazamiento en TUIG sugieren un mecanismo focal inverso (f = 150°; d = 70°; l = 90°). En la misma región ocurrió un sismo destructivo el 26 de agosto de 1959 (Mw6.4), a una profundidad similar y con un mecanismo similar. El análisis del sismo de 1997 refuerza la conclusión anterior de que la corteza inferior bajo la cuenca del Coatzacoalcos-Minatitlán, está en un régimen de esfuerzos de fallamiento inverso, en contraste con la parte superficial de la corteza que se caracteriza por un fallamiento normal; esto implica una permutación con la profundidad de los esfuerzos principales máximo y mínimo. Esto está de acuerdo con las observaciones, en otros sitios, que el estado de esfuerzos en las cuencas sedimentarias pueden ser diferentes del que se tiene a mayor profundidad.Mecanismos focales están disponibles para siete sismos en y cerca del Golfo de México. Todos estos eventos muestran en la región una corteza media y baja en un régimen de fallamiento inverso. La tendencia observada de los ejes P de estos sismos se puede explicar por una o más de las siguientes causas: acoplamiento fuerte a lo largo de la interfase de la placa en subducción fuera de la costa en Tehuantepec; el movimiento absoluto de la placa de América del Norte; y el hundimiento de la litosfera debido a la acumulación de la carga de los sedimentos.Usamos los registros del sismo de 1997 como función de Green empírica para simular los movimientos de tierra en la región epicentral de un sismo de Mw6.4 postulado en la cuenca Comalcalco. Bajo supuestos razonables, los valores esperados de aceleración, velocidad y desplazamiento picos son 120-260 gales, 12 a 28cm/s, y 6 a 11cm, respectivamente. La extensa licuefacción reportada en Coatzacoalcos durante el sismo de 1959, Mw6.4, sugiere que los sedimentos de la cuenca se comportan de manera no lineal bajo tal excitación." ] "en" => array:2 [ "titulo" => "Abstract" "resumen" => "We analyze the 6 September 1997Mw4.5 earthquake, which occurred about 25km SE of Coatzacoalcos, Veracruz. The earthquake was recorded by the local broadband station TUIG (S-P time = 5 s). P-wave polarities at regional and teleseismic distances and modeling of the displacement waveforms at TUIG yields a thrust-faulting focal mechanism (f = 150°; d = 70°; l = 90°). In the same region a destructive Mw6.4 earthquake occurred on 26 August 1959 at a similar depth and with a similar mechanism. The analysis of the 1997 event reinforces a previous conclusion that the lower crust beneath the Comalcalco basin is in a thrust-faulting stress regime, in contrast to the shallow part of the crust, which is characterized by normal-faulting; this implies a permutation with depth of the maximum and minimum principal stresses. It agrees with observations elsewhere that the state of stress in sedimentary basins can be different from the one at greater depth.Focal mechanisms are available for seven earthquakes in and near the Gulf of Mexico. All of these events indicate a thrust-faulting type stress regime at mid- and lower-crustal levels. The observed trend of the P axes of these earthquakes can be explained by one or more of the following causes: strong coupling along the subduction plate interface offshore Tehuantepec; absolute motion of the North American plate; and downwarping of the lithosphere due to sediment loading.By using the recordings of the 1997 event as empirical Green's function, we simulate the ground motions in the epicentral region of a postulated Mw6.4 earthquake in the Comalcalco basin. Under reasonable assumptions, the expected peak acceletion, velocity and displacement are 120-260gal, 12-28cm/s, and 6-11cm, respectively. The extensive soil liquefaction in Coatzacoalcos during the 1959, Mw6.4, earthquake suggests that the sediments of the basin behave nonlinearly under such excitation." ] ] "multimedia" => array:11 [ 0 => array:7 [ "identificador" => "fig0005" "etiqueta" => "Figure 1" "tipo" => "MULTIMEDIAFIGURA" "mostrarFloat" => true "mostrarDisplay" => false "figura" => array:1 [ 0 => array:4 [ "imagen" => "gr1.jpeg" "Alto" => 1096 "Ancho" => 1183 "Tamanyo" => 233097 ] ] "descripcion" => array:1 [ "en" => "Earthquakes in and near Gulf of Mexico with known focal mechanism. Source parameters of the events are listed in <a class="elsevierStyleCrossRef" href="#tbl0010">Table 2</a>. Focal mechanisms show that the mid- and lower crust of the Gulf is under compressive stress regime. Dotted lines indicate the bathymetry of the Gulf and gray dashed lines denote the limits of the buried salt deposits. LVPP = Laguna Verde Power Plant. Triangle shows location of station TUIG." ] ] 1 => array:7 [ "identificador" => "fig0010" "etiqueta" => "Figure 2" "tipo" => "MULTIMEDIAFIGURA" "mostrarFloat" => true "mostrarDisplay" => false "figura" => array:1 [ 0 => array:4 [ "imagen" => "gr2.jpeg" "Alto" => 573 "Ancho" => 1872 "Tamanyo" => 132680 ] ] "descripcion" => array:1 [ "en" => "Seismograms at station TUIG during the 6 September 1997 earthquake. (a) Acceleration, (b) velocity, and (c) displacement. The traces in (b) and (c) have been obtained by integration of the accelerograms shown in (a)." ] ] 2 => array:7 [ "identificador" => "fig0015" "etiqueta" => "Figure 3" "tipo" => "MULTIMEDIAFIGURA" "mostrarFloat" => true "mostrarDisplay" => false "figura" => array:1 [ 0 => array:4 [ "imagen" => "gr3.jpeg" "Alto" => 877 "Ancho" => 882 "Tamanyo" => 88986 ] ] "descripcion" => array:1 [ "en" => "Initial part of the three components of displacement at TUIG. The horizontal components have been multiplied by 20." ] ] 3 => array:7 [ "identificador" => "fig0020" "etiqueta" => "Figure 4" "tipo" => "MULTIMEDIAFIGURA" "mostrarFloat" => true "mostrarDisplay" => false "figura" => array:1 [ 0 => array:4 [ "imagen" => "gr4.jpeg" "Alto" => 1313 "Ancho" => 1351 "Tamanyo" => 189743 ] ] "descripcion" => array:1 [ "en" => "(Top) P-wave first motions of the 1997 earthquake plotted on lower-hemisphere, equal-area projection. With the exception of TUIG, all Mexican broadband stations recorded dilatation (open circles). Three teleseismic stations and TUIG show compression (solid circles). Focal mechanism, f = 150°; d = 70°; l = 90°, which satisfies first-motion data, and the waveform at TUIG is shown. (Bottom, left) Comparison of observed and infinite-space synthetic seismograms at station TUIG. (Bottom, right) Comparison of observed and synthetic seismograms at station TUIG. Synthetics were computed using crustal model and focal parameters given in <a class="elsevierStyleCrossRefs" href="#tbl0005">Tables 1 and 2</a>, respectively." ] ] 4 => array:7 [ "identificador" => "fig0025" "etiqueta" => "Figure 5" "tipo" => "MULTIMEDIAFIGURA" "mostrarFloat" => true "mostrarDisplay" => false "figura" => array:1 [ 0 => array:4 [ "imagen" => "gr5.jpeg" "Alto" => 588 "Ancho" => 1869 "Tamanyo" => 148314 ] ] "descripcion" => array:1 [ "en" => "An example of simulated acceleration, velocity, and displacement traces in the epicentral region from a postulated Mw6.5 earthquake, using recording of the 1997 earthquake as empirical Green's function (stress drop of EGF = stress drop of target earthquake = 6MPa). The right frame also shows, by dashed lines, the deterministic, synthetic displacement seismograms at TUIG for an Mw6.5 earthquake located at the focus of the 1997 event." ] ] 5 => array:7 [ "identificador" => "tbl0005" "etiqueta" => "Table 1" "tipo" => "MULTIMEDIATABLA" "mostrarFloat" => true "mostrarDisplay" => false "tabla" => array:1 [ "tablatextoimagen" => array:1 [ 0 => array:2 [ "tabla" => array:1 [ 0 => """ <table border="0" frame="\n \t\t\t\t\tvoid\n \t\t\t\t" class=""><thead title="thead"><tr title="table-row"><th class="td" title="table-head " align="left" valign="top" scope="col" style="border-bottom: 2px solid black">Layer \t\t\t\t\t\t\n \t\t\t\t</th><th class="td" title="table-head " align="left" valign="top" scope="col" style="border-bottom: 2px solid black">Thickness km \t\t\t\t\t\t\n \t\t\t\t</th><th class="td" title="table-head " align="left" valign="top" scope="col" style="border-bottom: 2px solid black">P-wave speed α, km/s \t\t\t\t\t\t\n \t\t\t\t</th><th class="td" title="table-head " align="left" valign="top" scope="col" style="border-bottom: 2px solid black">S-wave speed β, km/s \t\t\t\t\t\t\n \t\t\t\t</th><th class="td" title="table-head " align="left" valign="top" scope="col" style="border-bottom: 2px solid black">Density gm/cm3 \t\t\t\t\t\t\n \t\t\t\t</th><th class="td" title="table-head " align="left" valign="top" scope="col" style="border-bottom: 2px solid black">Quality Qa \t\t\t\t\t\t\n \t\t\t\t</th><th class="td" title="table-head " align="left" valign="top" scope="col" style="border-bottom: 2px solid black">Factor Qβ \t\t\t\t\t\t\n \t\t\t\t</th></tr></thead><tbody title="tbody"><tr title="table-row"><td class="td-with-role" title="table-entry ; entry_with_role_rowhead " align="left" valign="top">1 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">1.8 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">2.80 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">1.40 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">2.70 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">80 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">40 \t\t\t\t\t\t\n \t\t\t\t</td></tr><tr title="table-row"><td class="td-with-role" title="table-entry ; entry_with_role_rowhead " align="left" valign="top">2 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">15.6 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">4.25 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">2.40 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">2.80 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">300 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">200 \t\t\t\t\t\t\n \t\t\t\t</td></tr><tr title="table-row"><td class="td-with-role" title="table-entry ; entry_with_role_rowhead " align="left" valign="top">3 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">∞ \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">6.50 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">3.75 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">2.85 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">400 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">300 \t\t\t\t\t\t\n \t\t\t\t</td></tr></tbody></table> """ ] "imagenFichero" => array:1 [ 0 => "xTab890459.png" ] ] ] ] "descripcion" => array:1 [ "en" => "Crustal model near Coatzacoalcos used in the synthesis of ground motion." ] ] 6 => array:7 [ "identificador" => "tbl0010" "etiqueta" => "Table 2" "tipo" => "MULTIMEDIATABLA" "mostrarFloat" => true "mostrarDisplay" => false "tabla" => array:2 [ "leyenda" => "a Location from International Seismological Summary, ISS; depth, focal mechanism, and Mw from <a class="elsevierStyleCrossRef" href="#bib0125">Suárez (2000)</a>.b Location from International Seismological Centre, ISC; depth, focal mechanism, and Mw from <a class="elsevierStyleCrossRef" href="#bib0125">Suárez (2000)</a>.c Location, depth, and focal mechanism from <a class="elsevierStyleCrossRef" href="#bib0050">Frohlich (1982)</a>. The two mechanisms are extreme types consistent with first-motion data.d This study.e Global Centroid Moment Tensor (CMT) catalog.f Source parameters listed in http://www.eas.slu.edu/eqc/eqc_mt/MECH.NA/20070523190916/index.htmlg<a class="elsevierStyleCrossRef" href="#bib0045">Franco et al. (2013)</a>" "tablatextoimagen" => array:1 [ 0 => array:2 [ "tabla" => array:1 [ 0 => """ <table border="0" frame="\n \t\t\t\t\tvoid\n \t\t\t\t" class=""><thead title="thead"><tr title="table-row"><th class="td" title="table-head " align="left" valign="top" scope="col" style="border-bottom: 2px solid black">No. \t\t\t\t\t\t\n \t\t\t\t</th><th class="td" title="table-head " align="left" valign="top" scope="col" style="border-bottom: 2px solid black">Date \t\t\t\t\t\t\n \t\t\t\t</th><th class="td" title="table-head " align="left" valign="top" scope="col" style="border-bottom: 2px solid black">Latitude °N \t\t\t\t\t\t\n \t\t\t\t</th><th class="td" title="table-head " align="left" valign="top" scope="col" style="border-bottom: 2px solid black">Longitude °W \t\t\t\t\t\t\n \t\t\t\t</th><th class="td" title="table-head " align="left" valign="top" scope="col" style="border-bottom: 2px solid black">Depth km \t\t\t\t\t\t\n \t\t\t\t</th><th class="td" title="table-head " align="left" valign="top" scope="col" style="border-bottom: 2px solid black">Mw \t\t\t\t\t\t\n \t\t\t\t</th><th class="td" title="table-head " align="left" valign="top" scope="col" style="border-bottom: 2px solid black">Focal Mechanism ϕ’° \t\t\t\t\t\t\n \t\t\t\t</th><th class="td" title="table-head " align="left" valign="top" scope="col" style="border-bottom: 2px solid black">δ’° \t\t\t\t\t\t\n \t\t\t\t</th><th class="td" title="table-head " align="left" valign="top" scope="col" style="border-bottom: 2px solid black">λ’° \t\t\t\t\t\t\n \t\t\t\t</th></tr></thead><tbody title="tbody"><tr title="table-row"><td class="td-with-role" title="table-entry ; entry_with_role_rowhead " align="left" valign="top">1a \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">26 Aug 1959 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">18.26 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">94.43 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">21 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">6.4 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">309 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">32 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">102 \t\t\t\t\t\t\n \t\t\t\t</td></tr><tr title="table-row"><td class="td-with-role" title="table-entry ; entry_with_role_rowhead " align="left" valign="top">2b \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">11 Mar 1967 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">19.23 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">95.74 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">26 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">5.7 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">250 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">39 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">20 \t\t\t\t\t\t\n \t\t\t\t</td></tr><tr title="table-row"><td class="td-with-role" title="table-entry ; entry_with_role_rowhead " align="left" valign="top">3c \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">24 Jul 1978 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">26.49 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">88.79 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">15 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">5.0 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">225 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">49 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">111 \t\t\t\t\t\t\n \t\t\t\t</td></tr><tr title="table-row"><td class="td" title="table-entry " align="" valign="top"> \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="" valign="top"> \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="" valign="top"> \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="" valign="top"> \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="" valign="top"> \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="" valign="top"> \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">240 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">63 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">52 \t\t\t\t\t\t\n \t\t\t\t</td></tr><tr title="table-row"><td class="td-with-role" title="table-entry ; entry_with_role_rowhead " align="left" valign="top">4d \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">06 Sep 1997 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">18.08 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">94.47 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">30 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">4.5 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">330 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">20 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">90 \t\t\t\t\t\t\n \t\t\t\t</td></tr><tr title="table-row"><td class="td-with-role" title="table-entry ; entry_with_role_rowhead " align="left" valign="top">5e \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">10 Sep 2006 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">26.32 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">86.84 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">30 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">5.9 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">324 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">28 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">117 \t\t\t\t\t\t\n \t\t\t\t</td></tr><tr title="table-row"><td class="td-with-role" title="table-entry ; entry_with_role_rowhead " align="left" valign="top">6e \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">23 May 2007 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">21.98 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">96.31 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">24 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">5.6 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">102 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">80 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">-1 \t\t\t\t\t\t\n \t\t\t\t</td></tr><tr title="table-row"><td class="td" title="table-entry " align="" valign="top"> \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="" valign="top"> \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">(22.02 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">96.27 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">11 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">5.6 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">95 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">71 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">-16)f \t\t\t\t\t\t\n \t\t\t\t</td></tr><tr title="table-row"><td class="td" title="table-entry " align="" valign="top"> \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="" valign="top"> \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">(21.98 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">96.14 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">44 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">5.5 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">106 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">83 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">8)g \t\t\t\t\t\t\n \t\t\t\t</td></tr><tr title="table-row"><td class="td-with-role" title="table-entry ; entry_with_role_rowhead " align="left" valign="top">7e \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">29 Oct 2009 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">19.14 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">95.58 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">17 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">5.7 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">310 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">25 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">59 \t\t\t\t\t\t\n \t\t\t\t</td></tr><tr title="table-row"><td class="td" title="table-entry " align="" valign="top"> \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="" valign="top"> \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">(18.95 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">95.69 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">16 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">5.4 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">288 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">26 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">4)g \t\t\t\t\t\t\n \t\t\t\t</td></tr></tbody></table> """ ] "imagenFichero" => array:1 [ 0 => "xTab890461.png" ] ] ] ] "descripcion" => array:1 [ "en" => "Source parameters of earthquakes in and near Gulf of Mexico." ] ] 7 => array:7 [ "identificador" => "tbl0015" "etiqueta" => "Table 3" "tipo" => "MULTIMEDIATABLA" "mostrarFloat" => true "mostrarDisplay" => false "tabla" => array:1 [ "tablatextoimagen" => array:1 [ 0 => array:2 [ "tabla" => array:1 [ 0 => """ <table border="0" frame="\n \t\t\t\t\tvoid\n \t\t\t\t" class=""><thead title="thead"><tr title="table-row"><th class="td" title="table-head " align="left" valign="top" scope="col" style="border-bottom: 2px solid black">Stres Drop, MPa EFG/Target \t\t\t\t\t\t\n \t\t\t\t</th><th class="td" title="table-head " align="left" valign="top" scope="col" style="border-bottom: 2px solid black">PGA, N \t\t\t\t\t\t\n \t\t\t\t</th><th class="td" title="table-head " align="left" valign="top" scope="col" style="border-bottom: 2px solid black">cm/s2 E \t\t\t\t\t\t\n \t\t\t\t</th><th class="td" title="table-head " align="left" valign="top" scope="col" style="border-bottom: 2px solid black">Z \t\t\t\t\t\t\n \t\t\t\t</th><th class="td" title="table-head " align="left" valign="top" scope="col" style="border-bottom: 2px solid black">PGV, N \t\t\t\t\t\t\n \t\t\t\t</th><th class="td" title="table-head " align="left" valign="top" scope="col" style="border-bottom: 2px solid black">cm/s E \t\t\t\t\t\t\n \t\t\t\t</th><th class="td" title="table-head " align="left" valign="top" scope="col" style="border-bottom: 2px solid black">Z \t\t\t\t\t\t\n \t\t\t\t</th><th class="td" title="table-head " align="left" valign="top" scope="col" style="border-bottom: 2px solid black">PGD, N \t\t\t\t\t\t\n \t\t\t\t</th><th class="td" title="table-head " align="left" valign="top" scope="col" style="border-bottom: 2px solid black">cm E \t\t\t\t\t\t\n \t\t\t\t</th><th class="td" title="table-head " align="left" valign="top" scope="col" style="border-bottom: 2px solid black">Z \t\t\t\t\t\t\n \t\t\t\t</th></tr></thead><tbody title="tbody"><tr title="table-row"><td class="td-with-role" title="table-entry ; entry_with_role_rowhead " align="left" valign="top">6/6 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">146 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">173 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">103 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">13.2 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">18.7 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">6.8 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">8.8 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">6.5 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">6.1 \t\t\t\t\t\t\n \t\t\t\t</td></tr><tr title="table-row"><td class="td-with-role" title="table-entry ; entry_with_role_rowhead " align="left" valign="top">6/12 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">213 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">262 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">161 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">20.0 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">27.6 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">9.2 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">10.7 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">7.2 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">6.4 \t\t\t\t\t\t\n \t\t\t\t</td></tr><tr title="table-row"><td class="td-with-role" title="table-entry ; entry_with_role_rowhead " align="left" valign="top">12/12 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">171 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">198 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">124 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">17.9 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">25.8 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">8.7 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">10.6 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">7.1 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">6.3 \t\t\t\t\t\t\n \t\t\t\t</td></tr><tr title="table-row"><td class="td-with-role" title="table-entry ; entry_with_role_rowhead " align="left" valign="top">12/6 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">121 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">127 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">88 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">11.8 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">17.5 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">6.0 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">8.5 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">6.4 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">6.0 \t\t\t\t\t\t\n \t\t\t\t</td></tr></tbody></table> """ ] "imagenFichero" => array:1 [ 0 => "xTab890460.png" ] ] ] ] "descripcion" => array:1 [ "en" => "Simulated peak ground motions for a postulated Mw6.4 earthquake using recordings of the 1997 earthquake as EGF." ] ] 8 => array:6 [ "identificador" => "eq0005" "etiqueta" => "(1)" "tipo" => "MULTIMEDIAFORMULA" "mostrarFloat" => false "mostrarDisplay" => true "Formula" => array:1 [ "imagen" => array:1 [ 0 => array:4 [ "Fichero" => "fx1.jpeg" "Tamanyo" => 23991 "Alto" => 86 "Ancho" => 1131 ] ] ] ] 9 => array:6 [ "identificador" => "eq0010" "etiqueta" => "(2)" "tipo" => "MULTIMEDIAFORMULA" "mostrarFloat" => false "mostrarDisplay" => true "Formula" => array:1 [ "imagen" => array:1 [ 0 => array:4 [ "Fichero" => "fx2.jpeg" "Tamanyo" => 24841 "Alto" => 88 "Ancho" => 1039 ] ] ] ] 10 => array:6 [ "identificador" => "eq0015" "etiqueta" => "(3)" "tipo" => "MULTIMEDIAFORMULA" "mostrarFloat" => false "mostrarDisplay" => true "Formula" => array:1 [ "imagen" => array:1 [ 0 => array:4 [ "Fichero" => "fx3.jpeg" "Tamanyo" => 56010 "Alto" => 88 "Ancho" => 1022 ] ] ] ] ] "bibliografia" => array:2 [ "titulo" => "References" "seccion" => array:1 [ 0 => array:2 [ "identificador" => "bibs0005" "bibliografiaReferencia" => array:29 [ 0 => array:3 [ "identificador" => "bib0005" "etiqueta" => "Astiz and Kanamori, 1984" "referencia" => array:1 [ 0 => array:2 [ "contribucion" => array:1 [ 0 => array:2 [ "titulo" => "An earthquake doublet in Ometepec, Guerrero" "autores" => array:1 [ 0 => array:2 [ "etal" => false "autores" => array:2 [ 0 => "L. 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"vista" => "all" ] ] ] "idiomaDefecto" => "en" "url" => "/00167169/0000005400000003/v2_201509120041/S0016716915000306/v2_201509120041/en/main.assets" "Apartado" => array:4 [ "identificador" => "40021" "tipo" => "SECCION" "en" => array:2 [ "titulo" => "Articles" "idiomaDefecto" => true ] "idiomaDefecto" => "en" ] "PDF" => "https://static.elsevier.es/multimedia/00167169/0000005400000003/v2_201509120041/S0016716915000306/v2_201509120041/en/main.pdf?idApp=UINPBA00004N&text.app=https://www.elsevier.es/" "EPUB" => "https://multimedia.elsevier.es/PublicationsMultimediaV1/item/epub/S0016716915000306?idApp=UINPBA00004N"]

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Shri Krishna Singha,

Corresponding author

krishnamex@yahoo.com

Corresponding author.

, José Francisco Pachecob, Xyoli Pérez-Camposa, Mario Ordazc, Eduardo Reinosoc

a Instituto de Geofísica Universidad Nacional Autónoma de México Ciudad Universitaria Delegación Coyoacán, 04510, México D.F., México

b Observatorio Vulcanológico y Sismológico de Costa Rica Universidad Nacional

c Instituto de Ingeniería Universidad Nacional Autónoma de México Ciudad Universitaria Delegación Coyoacán, 04510, México D.F., México

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    "titulo" => "The 6 September 1997 &#40;<span class="elsevierStyleItalic">M</span><span class="elsevierStyleInf">w</span>4&#46;5&#41; Coatzacoalcos-Minatitl&#225;n&#44; Veracruz&#44; Mexico earthquake&#58; implications for tectonics and seismic hazard of the region"
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          "en" => "<p id="spar0040" class="elsevierStyleSimplePara elsevierViewall">Seismograms at station TUIG during the 6 September 1997 earthquake&#46; &#40;a&#41; Acceleration&#44; &#40;b&#41; velocity&#44; and &#40;c&#41; displacement&#46; The traces in &#40;b&#41; and &#40;c&#41; have been obtained by integration of the accelerograms shown in &#40;a&#41;&#46;</p>"
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    "textoCompleto" => "<span class="elsevierStyleSections"><span id="sec0005" class="elsevierStyleSection elsevierViewall"><span class="elsevierStyleSectionTitle" id="sect0025">Introduction</span><p id="par0005" class="elsevierStylePara elsevierViewall">A detailed analysis of the <span class="elsevierStyleItalic">M</span><span class="elsevierStyleInf">w</span>4&#46;5 earthquake of 6 September 1997&#44; which occurred near Coatzacoalcos-Minatitl&#225;n&#44; Veracruz&#44; is of interest for three reasons&#46; First&#44; the surface and the near-surface information from volcanic alignments&#44; borehole elongations&#44; and unpublished PEMEX seismic sections points to active normal-faulting in the region &#40;<a class="elsevierStyleCrossRef" href="#bib0130">Suter&#44; 1991</a>&#41;&#46; The focal mechanism of an earthquake which occurred nearby on 26 August 1959 &#40;<span class="elsevierStyleItalic">M</span><span class="elsevierStyleInf">w</span>6&#46;4&#41;&#44; however&#44; shows thrust faulting at a depth of about 26<span class="elsevierStyleHsp" style=""></span>km &#40;<a class="elsevierStyleCrossRefs" href="#bib0135">Wickens and Hodgson&#44; 1967&#59; Su&#225;rez&#44; 2000</a>&#59; see <a class="elsevierStyleCrossRef" href="#fig0005">Figure 1</a>&#41;&#46; It is&#44; therefore&#44; of interest to know whether the 1997 earthquake confirms such a change in the stress regime &#40;permutation of the least and maximum principal stresses&#41; with depth in the region&#46; In most regions&#44; the stress regime at relatively shallow depth agrees with that at mid-crustal depth&#46; There are some exceptions &#40;see&#44; e&#46;g&#46;&#44; Zoback and Zoback&#44; 1991&#41; and one such exception appears to be the coastal plain of the Gulf of Mexico &#40;<a class="elsevierStyleCrossRef" href="#bib0050">Frohlich&#44; 1982</a>&#59; Zoback and Zoback&#44; 1991&#59; <a class="elsevierStyleCrossRef" href="#bib0130">Suter&#44; 1991</a>&#41;&#46; Another classical example is the decoupling of the stress field across the basal detachment of the Jura fold-thrust belt&#59; the near-surface stress field is different from that in the basement &#40;<a class="elsevierStyleCrossRef" href="#bib0010">Becker <span class="elsevierStyleItalic">et al</span>&#46;&#44; 1987</a>&#41;&#46;</p><elsevierMultimedia ident="fig0005"></elsevierMultimedia><p id="par0010" class="elsevierStylePara elsevierViewall">Second&#44; the earthquake of 26 August 1959 caused serious damage to the towns of J&#225;ltipan&#44; Coatzacoalcos&#44; and Minatitl&#225;n &#40;<a class="elsevierStyleCrossRefs" href="#bib0035">Figueroa&#44; 1964&#59; Rosenblueth&#44; 1964</a>&#59; Res&#233;n-diz&#44; 1964&#41;&#46; The latter two towns have beco-me important industrial centers related to the intense activity of PEMEX&#44; the national petroleum company&#44; and population has grown by 22&#37; in the last 10 years to reach more than half million people &#40;<a class="elsevierStyleCrossRef" href="#bib0055">INEGI&#44; 2010</a>&#41;&#46; For this reason&#44; it is important to estimate ground motions that may be expected in these towns if an earthquake&#44; such as that of 1959&#44; were to recur in the region&#46; We may use the records of the 1997 earthquakes obtained at the near-source broadband station of TUIG as empirical Green&#39;s function to simulate the corresponding motions from an <span class="elsevierStyleItalic">M</span><span class="elsevierStyleInf">w</span>6&#46;4 event&#46; Although the station is about 25<span class="elsevierStyleHsp" style=""></span>km SE of Coatzacoalcos-Minatitl&#225;n&#44; the geology of these sites is roughly similar&#59; to a first approximation&#44; the results for the TUIG site may be valid for the entire region in case of an earthquake at about the same focal distance from TUIG as the event of 1997&#46;</p><p id="par0015" class="elsevierStylePara elsevierViewall">Finally&#44; a study of the 1997 earthquake &#40;and other events in and along the Gulf of Mexico&#41; has an important bearing on the seismic safety of the Laguna Verde nuclear power plant &#40;<a class="elsevierStyleCrossRef" href="#fig0005">Figure 1</a>&#41; as well as the hydrocarbon exploration and production facilities in this region&#46;</p></span><span id="sec0010" class="elsevierStyleSection elsevierViewall"><span class="elsevierStyleSectionTitle" id="sect0030">Data and analysis</span><p id="par0020" class="elsevierStylePara elsevierViewall">The 1997 earthquake was recorded by the local broadband station TUIG &#40;S-P time &#61; 5 s&#41; and by seven other broadband stations of the National Seismological Service &#40;SSN&#41;&#44; which were located at epicentral distances greater than 260<span class="elsevierStyleHsp" style=""></span>km&#46; The reported coda-wave magnitude&#44; <span class="elsevierStyleItalic">M</span><span class="elsevierStyleInf"><span class="elsevierStyleItalic">c</span></span>&#44; is 4&#46;3&#46; The epicenter of the event&#44; given by the SSN&#44; is 18&#46;146 &#176;N and 94&#46;499 &#176;W&#46; However&#44; its focal depth could not be constrained&#46; The epicenter and focal depth reported by the National Earthquake Information Center &#40;NEIC&#41;&#44; U&#46;S&#46; Geological Survey&#44; are 18&#46;017 &#176;N and 94&#46;396 &#176;W and 33<span class="elsevierStyleHsp" style=""></span>km&#44; respectively&#46; This depth was fixed by NEIC in the location of the earthquake&#46;</p><p id="par0025" class="elsevierStylePara elsevierViewall">For moderate Mexican earthquakes it is now possible to obtain a regional centroid moment tensor &#40;CMT&#41; solution using relatively long-period regional waveforms &#40;see&#44; e&#46;g&#46;&#44; <a class="elsevierStyleCrossRef" href="#bib0090">Pacheco and Singh&#44; 1998</a>&#41;&#46; Unfortunately&#44; the seismograms of the 1997 earthquake show little energy at periods greater than 10 s because of its relatively small magnitude&#46; At shorter periods&#44; a detailed three-dimensional crustal structure is needed to model the observed seismograms but is currently lacking for the region&#46; For these reasons it was not possible to obtain a CMT solution by inverting the regional waveforms&#46;</p><p id="par0030" class="elsevierStylePara elsevierViewall">A single&#44; near-source&#44; three-component broadband recording can be used to find a reliable location&#44; origin time&#44; and focal mechanism of an earthquake&#44; provided that a rough initial guess of the mechanism is available from other data &#40;see&#44; e&#46;g&#46;&#44; <a class="elsevierStyleCrossRefs" href="#bib0060">Kanamori <span class="elsevierStyleItalic">et al</span>&#46;&#44; 1990&#59; Singh <span class="elsevierStyleItalic">et al</span>&#46;&#44; 1997&#44; 2000a</a>&#41;&#46; The calculation of the location and origin time requires clear first arrivals on each of the three components of the ground motion as well as the knowledge of the local crustal structure&#46; <a class="elsevierStyleCrossRef" href="#fig0010">Figure 2</a> shows acceleration&#44; velocity and displacement traces at TUIG during the 6 September 1997 earthquake&#46; <a class="elsevierStyleCrossRef" href="#fig0015">Figure 3</a> illustrates the initial part of the three components of displacement at TUIG&#46; Note that the horizontal components have been amplified by a factor of 20&#46; The incidence of initial P-wave at the station is nearly vertical&#46; Nevertheless&#44; it can be seen that the station is located in the NW quadrant with respect to the source&#46; The amplitude towards west at time 0&#46;172 s is 3&#46;5 times that towards north&#46; It follows that the station azimuth&#44; &#966;<span class="elsevierStyleInf">s</span>&#44; is 286&#176;&#46; Before proceeding further with the analysis of the source parameters of this earthquake&#44; we summarize our knowledge of the local crustal structure&#46;</p><elsevierMultimedia ident="fig0010"></elsevierMultimedia><elsevierMultimedia ident="fig0015"></elsevierMultimedia></span><span id="sec0015" class="elsevierStyleSection elsevierViewall"><span class="elsevierStyleSectionTitle" id="sect0035">Crustal structure of the region</span><p id="par0035" class="elsevierStylePara elsevierViewall">The P-wave speed&#44; a&#44; in the shallow crust south and near Coatzacoalcos is available from exploration seismology carried out by PEMEX &#40;A&#46; Camargo&#44; personal communication&#44; 1997&#41;&#46; The crust consists of a 1&#46;8<span class="elsevierStyleHsp" style=""></span>km thick layer with a &#61; 2&#46;5<span class="elsevierStyleHsp" style=""></span>km&#47;s&#44; overlying a layer of a &#61; 4&#46;25<span class="elsevierStyleHsp" style=""></span>km&#47;s&#46; The thickness of the second layer exceeds 3&#46;4<span class="elsevierStyleHsp" style=""></span>km&#44; the maximum depth reached by boreholes&#46; Based on receiver function analysis&#44; <a class="elsevierStyleCrossRef" href="#bib0025">Cruz-Atienza &#40;2000&#41;</a> reports sediment thickness of 16<span class="elsevierStyleHsp" style=""></span>km below TUIG&#46; N&#46; Shapiro &#40;unpublished report&#41; inverted group velocity dispersion curve corresponding to the region between the City of Oaxaca and TUIG&#46; In the inversion&#44; Shapiro fixed the thickness of the first layer and a values of the first and the second layers to the values given by PEMEX&#46; The shear-wave speeds&#44; b&#44; of the first and second layers were taken as 1&#46;4<span class="elsevierStyleHsp" style=""></span>km&#47;s and 2&#46;4<span class="elsevierStyleHsp" style=""></span>km&#47;s&#44; respectively&#46; The crustal model adopted from the results of <a class="elsevierStyleCrossRef" href="#bib0025">Cruz-Atienza &#40;2000&#41;</a> and N&#46; Shapiro&#44; and used by us in generating synthetic seismograms&#44; is given in <a class="elsevierStyleCrossRef" href="#tbl0005">Table 1</a>&#46; In this table&#44; the densities and the quality factors&#44; <span class="elsevierStyleItalic">Q</span>&#44; of the layers have been taken arbitrarily&#59; the results are not very sensitive to their choices&#46;</p><elsevierMultimedia ident="tbl0005"></elsevierMultimedia></span><span id="sec0020" class="elsevierStyleSection elsevierViewall"><span class="elsevierStyleSectionTitle" id="sect0040">Source parameters of the earthquake</span><p id="par0040" class="elsevierStylePara elsevierViewall">Based on the crustal model in <a class="elsevierStyleCrossRef" href="#tbl0005">Table 1</a> and the &#40;S-P&#41; time of 5 s at station TUIG&#44; the maximum depth of the earthquake&#44; Hmax&#44; assuming the station to be located directly above the focus&#44; is 30&#46;9<span class="elsevierStyleHsp" style=""></span>km&#46; If the thickness of the second layer in <a class="elsevierStyleCrossRef" href="#tbl0005">Table 1</a> is taken as 10<span class="elsevierStyleHsp" style=""></span>km&#44; then Hmax becomes 34&#46;8<span class="elsevierStyleHsp" style=""></span>km&#46; Near-vertical incidence at TUIG may be a consequence of both small epicentral distance as compared to the source depth&#44; and refraction of waves caused by progressively lower seismic speeds near the surface&#46;</p><p id="par0045" class="elsevierStylePara elsevierViewall"><a class="elsevierStyleCrossRef" href="#fig0020">Figure 4</a>&#44; top&#44; shows P-wave first-motion polarities at those Mexican and teleseismic stations where they could be read unequivocally&#46; These data suggest a thrust-faulting earthquake with possible strike-slip component&#46; The first motion polarities provide some constrains on the azimuth &#40;140&#176; &#8804; f &#8804; 190&#176;&#41; and the dip &#40;45&#176; &#8804; &#948; &#8804; 85&#176;&#41; of one of the nodal planes but the rake&#44; l&#44; of this plane can vary between 35&#176; and 120&#176;&#46; To determine the focal mechanism&#44; we performed a waveform inversion of the displacement traces recorded at TUIG&#46; For the inversion the event was approximated by a point-source shear dislocation&#46; Synthetic seismograms include near- and intermediate-field contributions &#40;<a class="elsevierStyleCrossRef" href="#bib0115">Singh <span class="elsevierStyleItalic">et al</span>&#46;&#44; 2000a</a>&#41;&#46; The effect of the free surface is approximately taken into account by multiplying the infinite-space synthetics by two&#46; This approximation is acceptable if the epicentral distance&#44; &#916;&#44; is smaller than the depth&#44; <span class="elsevierStyleItalic">H</span>&#46; We took the sta-tion azimuth&#44; f<span class="elsevierStyleInf"><span class="elsevierStyleItalic">s</span></span>&#44; as 286&#176;&#44; the take-off angle from the source&#44; <span class="elsevierStyleItalic">i</span><span class="elsevierStyleInf"><span class="elsevierStyleItalic">h</span></span>&#44; as 170&#176;&#44; and the angle of incidence at the surface&#44; <span class="elsevierStyleItalic">i</span><span class="elsevierStyleInf"><span class="elsevierStyleItalic">O</span></span>&#44; as 5&#176; from the vertical&#46; Based on the observed P-pulse on the Z-component &#40;<a class="elsevierStyleCrossRef" href="#fig0010">Figure 2</a>c&#41;&#44; we chose a triangular source with duration&#44; t&#44; of 0&#46;38 s&#46; We varied the azimuth&#44; dip&#44; and rake within the ranges mentioned above&#46; No contradiction of the first motion polarities was allowed&#46; The two nodal planes obtained from the inversion are&#58; f &#61; 150&#176;&#59; d &#61; 70&#176;&#59; l &#61; 90&#176; and f &#61; 330&#176;&#59; d &#61; 20&#176;&#59; l &#61; 90&#176;&#46; The observed and synthetic seismograms are shown in the bottom left of <a class="elsevierStyleCrossRef" href="#fig0020">Figure 4</a>&#46;</p><elsevierMultimedia ident="fig0020"></elsevierMultimedia><p id="par0050" class="elsevierStylePara elsevierViewall">We generated synthetic seismograms corresponding to this focal mechanism and the crustal model given in <a class="elsevierStyleCrossRef" href="#tbl0005">Table 1</a>&#46; <a class="elsevierStyleCrossRef" href="#bib0020">Bouchon&#39;s &#40;1982&#41;</a> discrete wave number algorithm was used in the computation&#46; We again took f<span class="elsevierStyleInf"><span class="elsevierStyleItalic">s</span></span> &#61; 286&#176; and t &#61; 0&#46;38 s&#46; A good fit between observed and synthetic seismograms at TUIG was found for an epicentral distance of 7<span class="elsevierStyleHsp" style=""></span>km&#44; a depth of 30<span class="elsevierStyleHsp" style=""></span>km&#44; and <span class="elsevierStyleItalic">M</span><span class="elsevierStyleInf">0</span> &#61; 6&#46;0x1015 N-m &#40;<span class="elsevierStyleItalic">M</span><span class="elsevierStyleInf">w</span>4&#46;5&#41; &#40;<a class="elsevierStyleCrossRef" href="#fig0020">Figure 4</a>&#44; bottom right&#41;&#46; <a class="elsevierStyleCrossRef" href="#tbl0010">Table 2</a> summarizes the relevant source parameters of this earthquake&#46;</p><elsevierMultimedia ident="tbl0010"></elsevierMultimedia></span><span id="sec0025" class="elsevierStyleSection elsevierViewall"><span class="elsevierStyleSectionTitle" id="sect0045">Stress regime of the Gulf coast region of Coatzacoalcos-Minatitl&#225;n</span><p id="par0055" class="elsevierStylePara elsevierViewall">In spite of some uncertainty in its focal mechanism&#44; there is no doubt that the 1997 earthquake was a thrust event with&#44; probably&#44; some strike-slip component&#46; Its source was below the Comalcalco basin at a depth of about 30<span class="elsevierStyleHsp" style=""></span>km&#46; As mentioned earlier&#44; the surface and the near-surface information from volcanic alignments&#44; borehole elongations&#44; and unpublished PEMEX seismic sections in the Gulf coast basin region of Coatzacoalcos-Minatitl&#225;n suggest active normal-faulting in the upper few kilometers &#40;<a class="elsevierStyleCrossRef" href="#bib0130">Suter&#44; 1991</a>&#41;&#46; Thus&#44; there is a change of stress regime from extension in the sediments of the upper crust to shortening in the mid- and lower crust indicated by focal mechanisms &#40;<a class="elsevierStyleCrossRef" href="#fig0005">Figure 1</a>&#41;&#46; A similar change of stress regime with depth is reported in the central Gulf of Mexico by <a class="elsevierStyleCrossRef" href="#bib0050">Frohlich &#40;1982&#41;</a> from an analysis of an earthquake in 1978 at the edge of the Mississippi Fan at a depth of 15<span class="elsevierStyleHsp" style=""></span>km &#40;<a class="elsevierStyleCrossRef" href="#fig0005">Figure 1</a>&#41;&#46; Other cases of stress change below sedimentary basins are discussed in Zoback and Zoback &#40;1991&#41;&#46; Extension in upper part of crust is probably controlled by gravitational load and major topographic gradient&#44; at least in the adjacent Veracruz basin&#46;</p><p id="par0060" class="elsevierStylePara elsevierViewall"><a class="elsevierStyleCrossRef" href="#tbl0010">Table 2</a> lists seven intraplate earthquakes located in and near the Gulf of Mexico with known focal mechanisms&#46; It includes the earthquakes of 1978 and 1997&#46; The locations of these events and their focal mechanisms are illustrated in <a class="elsevierStyleCrossRef" href="#fig0005">Figure 1</a>&#46; For the earthquakes of 2007 and 2009&#44; more than one solution is available &#40;<a class="elsevierStyleCrossRef" href="#tbl0010">Table 2</a>&#41;&#46; For these two earthquakes&#44; the Global CMT location and focal mechanism is shown&#46; As most intraplate regions&#44; the Gulf is characterized by thrust-type stress regime &#40;<a class="elsevierStyleCrossRef" href="#bib0140">Zoback <span class="elsevierStyleItalic">et al</span>&#46;&#44; 1989</a>&#41;&#46; The orientations of the P-axes of the 1959&#44; 1967&#44; 2006&#44; 2007 and 2009 earthquakes range between N30&#176;E and N65&#176;E&#46; These are consistent with reported offshore stress orientations near the same region&#44; inferred from breakouts &#40;<a class="elsevierStyleCrossRefs" href="#bib0145">Zoback <span class="elsevierStyleItalic">et al</span>&#46;&#44; 1990&#59; Suter&#44; 1991</a>&#59; World Stress Map&#44; <a href="http://dc-app3-14.gfz-potsdam.de/">http&#58;&#47;&#47;dc-app3-14&#46;gfz-potsdam&#46;de&#47;</a>&#44; 12 May 2015&#41;&#46; These orientations fall between the directions of&#58; &#40;1&#41; the relative convergence of the Cocos and North American plates and &#40;2&#41; the absolute motion of the North American plate&#46; Perhaps both the relative convergence and the absolute motion are responsible for the observed P-axis&#44; with the former playing a more dominant role for events in and near the SSW Gulf due to their relative proximity to the middle America subduction zone &#40;earthquakes of 1959&#44; 1967&#44; 1997&#44; and 2009&#41; and the latter being dominant for the events of 2006 and 2007 which are relatively far from the plate boundary&#46; For the 2006 earthquake&#44; sliding of Sigsbee salt and landslide have also been suggested as possible causes &#40;<a class="elsevierStyleCrossRefs" href="#bib0080">Nettles&#44; 2007&#59; Franco <span class="elsevierStyleItalic">et al</span>&#46;&#44; 2013</a>&#41;&#46;</p><p id="par0065" class="elsevierStylePara elsevierViewall"><a class="elsevierStyleCrossRef" href="#bib0030">Dewey and Su&#225;rez &#40;1991&#41;</a> and <a class="elsevierStyleCrossRef" href="#bib0125">Su&#225;rez &#40;2000&#41;</a> suggest that the intraplate&#44; mid- and lower-crust compression below the Comalcalco basin&#44; as revealed by the 1959 and 1967 earthquakes&#44; may be a consequence of strong coupling along the plate interface where the Tehuantepec ridge subducts below Mexico&#46; This may also be true for the 1997 and 2009 earthquakes&#46; If so&#44; then&#44; unlike subduction of many other ridges &#40;<a class="elsevierStyleCrossRef" href="#bib0070">Kelleher and McCann&#44; 1976</a>&#41;&#44; the Tehuantepec ridge does not subduct aseismically&#46; Since there is no clear evidence for major&#47;great earthquakes in the Tehuantepec region during the last two centuries &#40;see&#44; e&#46;g&#46;&#44; <a class="elsevierStyleCrossRef" href="#bib0105">Singh <span class="elsevierStyleItalic">et al</span>&#46;&#44; 1981</a>&#41;&#44; it could mean that the recurrence period of such events in this segment is much greater than in other segments along the Mexican subduction zones where it is &#8764; 30 to 75 years &#40;<a class="elsevierStyleCrossRefs" href="#bib0105">Singh <span class="elsevierStyleItalic">et al</span>&#46;&#44; 1981&#59; Astiz and Kanamori&#44; 1984</a>&#41;&#46;</p><p id="par0070" class="elsevierStylePara elsevierViewall">As for the 1978 Mississippi Fan earthquake &#40;<a class="elsevierStyleCrossRef" href="#fig0005">Figure 1</a>&#41;&#44; the P-axis does not follow the trend of the other events&#46; The compressional nature of this earthquake was interpreted by <a class="elsevierStyleCrossRef" href="#bib0050">Frohlich &#40;1982&#41;</a> as a consequence of downwarping of the lithosphere due to sediment accumulation&#46;</p></span><span id="sec0030" class="elsevierStyleSection elsevierViewall"><span class="elsevierStyleSectionTitle" id="sect0050">Expected ground motions in the Coatzacoalcos-Minatitl&#225;n region from a postulated <span class="elsevierStyleItalic">M</span><span class="elsevierStyleInf">w</span>6&#46;4 earthquake</span><p id="par0075" class="elsevierStylePara elsevierViewall">The earthquake of 1959 destroyed a majority of the dwellings in the town of J&#225;ltipan &#40;<a class="elsevierStyleCrossRef" href="#bib0100">Rosenblueth&#44; 1964</a>&#41;&#46; Many buildings suffered structural or foundation failures in Coatzacoalcos and Minatitl&#225;n &#40;<a class="elsevierStyleCrossRefs" href="#bib0075">Marsal&#44; 1961&#59; Res&#233;ndiz&#44; 1964</a>&#41;&#46; The land near the port of Coatzacoalcos subsided&#46; Some of the effects of the earthquake were attributed to partial liquefaction of sand and silt &#40;<a class="elsevierStyleCrossRef" href="#bib0075">Marsal&#44; 1961</a>&#41;&#46; Modified Mercalli &#40;MM&#41; intensities in these towns during this earthquake were VIII &#40;<a class="elsevierStyleCrossRef" href="#bib0035">Figueroa&#44; 1964</a>&#41;&#46; The 1959 earthquake was not an isolated event&#46; The epicenter of the earthquake of 11 January&#44; 1946 was apparently close to that of 1959 &#40;<a class="elsevierStyleCrossRef" href="#bib0035">Figueroa&#44; 1964</a>&#41;&#46; The earthquake of 1946 was assigned a magnitude of 6&#46;0 &#40;<a class="elsevierStyleCrossRef" href="#bib0040">Figueroa&#44; 1970</a>&#41; and a MM intensity of VII in Coatzacoalcos &#40;<a class="elsevierStyleCrossRef" href="#bib0035">Figueroa&#44; 1964</a>&#41;&#46; The towns of Coatzacoalcos and Minatitl&#225;n are now important centers of national petroleum activity&#46; Thus&#44; it is of significant earthquake engineering interest to estimate the ground motions in these towns during a future local <span class="elsevierStyleItalic">M</span><span class="elsevierStyleInf">w</span>6&#46;4 earthquake&#46;</p><p id="par0080" class="elsevierStylePara elsevierViewall">To estimate the ground motions from an <span class="elsevierStyleItalic">M</span><span class="elsevierStyleInf">w</span>6&#46;4 earthquake&#44; we used the recording of 1997 earthquake as an empirical Green&#39;s function &#40;EGF&#41; and a method proposed by <a class="elsevierStyleCrossRef" href="#bib0085">Ordaz <span class="elsevierStyleItalic">et al</span>&#46; &#40;1995&#41;</a> which is based on adding <span class="elsevierStyleItalic">N</span> scaled EGF records&#44; each differed in time by a random delay&#46; The probability distribution of the delays is such that&#44; on average&#44; the simulations follow an w<span class="elsevierStyleSup">2</span>-spectral scaling at all frequencies&#46; The method requires specification of the seismic moment&#44; <span class="elsevierStyleItalic">M</span><span class="elsevierStyleInf">0</span>&#44; and the stress drop&#44; Ds&#44; of both the EGF and the target earthquake&#46; In our case&#44; <span class="elsevierStyleItalic">M</span><span class="elsevierStyleInf">0</span> of the EGF is 6x10<span class="elsevierStyleSup">15</span> N-m and that of the target event is 5x10<span class="elsevierStyleSup">18</span> N-m &#40;<span class="elsevierStyleItalic">M</span><span class="elsevierStyleInf">w</span>6&#46;4&#41;&#46; A rough estimate of the static stress drop of the EGF can be obtained from the following considerations&#46; For a circular rupture&#44; the radius&#44; <span class="elsevierStyleItalic">a</span>&#44; of the fault can be estimated by &#40;<a class="elsevierStyleCrossRef" href="#bib0015">Boatwright&#44; 1980</a>&#41;&#58;<elsevierMultimedia ident="eq0005"></elsevierMultimedia></p><p id="par0085" class="elsevierStylePara elsevierViewall">where t<span class="elsevierStyleInf">1&#47;2</span> is the rise time of the far-field pulse&#44; <span class="elsevierStyleItalic">v</span> is the rupture speed&#44; <span class="elsevierStyleItalic">c</span> is the wave speed&#44; and q is the take-off angle measured from fault normal&#46; For this event&#44; t<span class="elsevierStyleInf">1&#47;2</span> is about 0&#46;19 s &#40;<a class="elsevierStyleCrossRef" href="#tbl0010">Table 2</a>&#44; <a class="elsevierStyleCrossRef" href="#fig0010">Figure 2</a>c&#41;&#46; For S wave&#44; <span class="elsevierStyleItalic">c</span> &#61; b&#44; which we take as 3&#46;75<span class="elsevierStyleHsp" style=""></span>km&#47;s &#40;<a class="elsevierStyleCrossRef" href="#tbl0005">Table 1</a>&#41;&#46; Assuming f &#61; 330&#176;&#59; d &#61; 20&#176;&#59; l &#61; 90&#176; as the fault plane and <span class="elsevierStyleItalic">i</span><span class="elsevierStyleInf"><span class="elsevierStyleItalic">h</span></span> &#61;170&#176;&#44; q is &#8764;10&#176;&#46; For <span class="elsevierStyleItalic">v</span> &#61; 0&#46;9b&#44; we obtain a fault radius <span class="elsevierStyleItalic">a</span> &#61; 0&#46;76<span class="elsevierStyleHsp" style=""></span>km &#40;equation 1&#41;&#46; For a circular fault&#44; Ds is related to <span class="elsevierStyleItalic">M</span><span class="elsevierStyleInf">0</span> and <span class="elsevierStyleItalic">a</span> by &#40;<a class="elsevierStyleCrossRef" href="#bib0065">Keilis-Borok&#44; 1959</a>&#41;&#58;<elsevierMultimedia ident="eq0010"></elsevierMultimedia></p><p id="par0090" class="elsevierStylePara elsevierViewall">which gives Ds of &#8764; 6<span class="elsevierStyleHsp" style=""></span>MPa for the EGF&#46; In the simulations&#44; we take Ds of the EGF and the target event to be either 6<span class="elsevierStyleHsp" style=""></span>MPa or 12<span class="elsevierStyleHsp" style=""></span>MPa&#46; Typical simulated acceleration&#44; velocity&#44; and displacement traces&#44; corresponding to Ds &#61; 6<span class="elsevierStyleHsp" style=""></span>MPa for both events&#44; are illustrated in <a class="elsevierStyleCrossRef" href="#fig0025">Figure 5</a>&#46; In the figure&#44; we compare deterministic&#44; synthetic displacement seismograms with ones obtained by random summation of EGF&#46; The synthetics were generated at TUIG for an event with <span class="elsevierStyleItalic">M</span><span class="elsevierStyleInf">0</span> &#61; 5x10<span class="elsevierStyleSup">18</span> N-m &#40;<span class="elsevierStyleItalic">M</span><span class="elsevierStyleInf">w</span>6&#46;4&#41;&#44; located at the same focus as the 1997 earthquake&#44; and having the same focal mechanism&#46; The duration of the source time function&#44; t&#44; of Mexican earthquakes is related to their seismic moment by<elsevierMultimedia ident="eq0015"></elsevierMultimedia></p><elsevierMultimedia ident="fig0025"></elsevierMultimedia><p id="par0095" class="elsevierStylePara elsevierViewall">&#40;<a class="elsevierStyleCrossRef" href="#bib0120">Singh <span class="elsevierStyleItalic">et al</span>&#46;&#44; 2000b</a>&#41;&#46; Thus&#44; the estimated t for the target event is 4&#46;2 s&#46; A point source with a triangular source-time function of 4&#46;2 s duration and the crustal structure given in <a class="elsevierStyleCrossRef" href="#tbl0005">Table 1</a> were taken for the computation&#46; The <span class="elsevierStyleItalic">PGD</span> values are within a factor of two of each other&#46; Both calculations show important near-field contribution &#40;the ramp-like wave between P and S wave&#41;&#46;</p><p id="par0100" class="elsevierStylePara elsevierViewall">Results of simulation for various combinations of Ds are summarized in <a class="elsevierStyleCrossRef" href="#tbl0015">Table 3</a>&#46; The expected horizontal <span class="elsevierStyleItalic">PGA</span>&#44; <span class="elsevierStyleItalic">PGV</span>&#44; and <span class="elsevierStyleItalic">PGD</span> range between 120 and 260<span class="elsevierStyleHsp" style=""></span>gal&#44; 12 and 28<span class="elsevierStyleHsp" style=""></span>cm&#47;s&#44; and 6 and 11<span class="elsevierStyleHsp" style=""></span>cm&#44; respectively&#46;</p><elsevierMultimedia ident="tbl0015"></elsevierMultimedia><p id="par0105" class="elsevierStylePara elsevierViewall">Although the ground motions estimated by random summation of the EGF are reasonable&#44; there are several factors which introduce uncertainties in these results&#46; The stress drop of the EGF event is uncertain and that of the target earthquake is assumed&#46; The directivity of the source may give rise to greater or smaller ground motions than those computed by our method&#46; Finally&#44; a single EGF may not be adequate to sample the entire fault plane of an <span class="elsevierStyleItalic">M</span><span class="elsevierStyleInf">w</span>6&#46;4&#46;</p><p id="par0110" class="elsevierStylePara elsevierViewall">We emphasize that this synthesis of the ground motion is based on the assumption of linear elastic response of the sediments&#46; Almost certainly the shallow sediments of the Gulf basin will behave nonlinearly under such excitation&#44; as was the case during the 1959 earthquake&#46; In view of the uncertainties&#44; the observed ground motions may easily differ by a factor of 2 or 3 from the expected ones&#46; This however is usually the case in ground motion predictions&#46;</p></span><span id="sec0035" class="elsevierStyleSection elsevierViewall"><span class="elsevierStyleSectionTitle" id="sect0055">Conclusions</span><p id="par0115" class="elsevierStylePara elsevierViewall">Our analysis shows that the 6 September 1997 earthquake &#40;<span class="elsevierStyleItalic">H</span> &#61; 30<span class="elsevierStyleHsp" style=""></span>km&#59; <span class="elsevierStyleItalic">M</span><span class="elsevierStyleInf">w</span>4&#46;5&#41;&#44; like the nearby earthquake of 26 August 1957 &#40;<span class="elsevierStyleItalic">H</span> &#61; 21<span class="elsevierStyleHsp" style=""></span>km&#59; <span class="elsevierStyleItalic">M</span><span class="elsevierStyleInf">w</span>6&#46;4&#41;&#44; was a thrust event&#46; The event confirms a previous conclusion that while the upper sediments of the Gulf coast basins are in an extensional &#40;normal fault-type&#41; stress regime&#44; the mid- and lower crust is in a shortening &#40;thrust fault-type&#41; stress regime &#40;<a class="elsevierStyleCrossRefs" href="#bib0030">Dewey and Su&#225;rez&#44; 1991&#59; Suter&#44; 1991</a>&#41;&#44; which implies a permutation between the vertical and maximum horizontal principal stresses&#46; Upper crust is under extension probably because of gravitational loads and high topographic gradient&#59; the stress field of middle to lower crust may be controlled by far-field loads at convergent plate margin and&#47;or absolute plate motion&#46;</p><p id="par0120" class="elsevierStylePara elsevierViewall">Our estimation of ground motion in the epicentral region of Comalcalco basin due to a postulated <span class="elsevierStyleItalic">M</span><span class="elsevierStyleInf">w</span>6&#46;4 earthquake indicates that peak acceleration&#44; velocity&#44; and displacement &#40;assuming linear behavior of the sediments&#41; may be in the range of 120-260<span class="elsevierStyleHsp" style=""></span>gal&#44; 12-28<span class="elsevierStyleHsp" style=""></span>cm&#47;s&#44; and 6-11<span class="elsevierStyleHsp" style=""></span>cm&#44; respectively&#46; These&#44; then&#44; are also our estimations of the ground motions during the 1959&#44; <span class="elsevierStyleItalic">M</span><span class="elsevierStyleInf">w</span>6&#46;4&#44; earthquake&#46; These estimations were obtained using 6 September 1997 event as an empirical Green&#39;s function under various simplifying&#44; though reasonable&#44; assumptions&#46; They are valid for sites with local geology similar to that of station TUIG&#46; The estimation of ground motions at other nearby sites&#44; such as Minatitl&#225;n&#44; may be calculated if their site responses are known&#46; Subjected to such ground motions the sediments of the Gulf Coast are likely to behave nonlinearly and may liquefy&#44; as was the case during the 1959 earthquake&#46;</p></span></span>"
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          "titulo" => "Stress regime of the Gulf coast region of Coatzacoalcos-Minatitl&#225;n"
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          "titulo" => "Expected ground motions in the Coatzacoalcos-Minatitl&#225;n region from a postulated M6&#46;4 earthquake"
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            1 => "movimientos fuertes"
            2 => "tect&#243;nica del Golfo de M&#233;xico"
            3 => "peligro s&#237;smico del Golfo de M&#233;xico&#46;"
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            1 => "strong motion"
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        "titulo" => "Resumen"
        "resumen" => "<span id="abst0005" class="elsevierStyleSection elsevierViewall"><p id="spar0005" class="elsevierStyleSimplePara elsevierViewall">Analizamos el sismo del 6 de septiembre de 1997 &#40;<span class="elsevierStyleItalic">M</span><span class="elsevierStyleInf">w</span>4&#46;5&#41;&#44; que se produjo a unos 25<span class="elsevierStyleHsp" style=""></span>km al SE de Coatzacoalcos&#44; Veracruz&#46; El sismo fue registrado por la estaci&#243;n local TUIG de banda ancha de &#40;tiempo S-P &#61; 5 s&#41;&#46; Las polaridades de la onda P a distancias regionales y teles&#237;smicas&#44; y el modelado de las formas de onda de desplazamiento en TUIG sugieren un mecanismo focal inverso &#40;f &#61; 150&#176;&#59; d &#61; 70&#176;&#59; l &#61; 90&#176;&#41;&#46; En la misma regi&#243;n ocurri&#243; un sismo destructivo el 26 de agosto de 1959 &#40;<span class="elsevierStyleItalic">M</span><span class="elsevierStyleInf">w</span>6&#46;4&#41;&#44; a una profundidad similar y con un mecanismo similar&#46; El an&#225;lisis del sismo de 1997 refuerza la conclusi&#243;n anterior de que la corteza inferior bajo la cuenca del Coatzacoalcos-Minatitl&#225;n&#44; est&#225; en un r&#233;gimen de esfuerzos de fallamiento inverso&#44; en contraste con la parte superficial de la corteza que se caracteriza por un fallamiento normal&#59; esto implica una permutaci&#243;n con la profundidad de los esfuerzos principales m&#225;ximo y m&#237;nimo&#46; Esto est&#225; de acuerdo con las observaciones&#44; en otros sitios&#44; que el estado de esfuerzos en las cuencas sedimentarias pueden ser diferentes del que se tiene a mayor profundidad&#46;</p><p id="spar0010" class="elsevierStyleSimplePara elsevierViewall">Mecanismos focales est&#225;n disponibles para siete sismos en y cerca del Golfo de M&#233;xico&#46; Todos estos eventos muestran en la regi&#243;n una corteza media y baja en un r&#233;gimen de fallamiento inverso&#46; La tendencia observada de los ejes P de estos sismos se puede explicar por una o m&#225;s de las siguientes causas&#58; acoplamiento fuerte a lo largo de la interfase de la placa en subducci&#243;n fuera de la costa en Tehuantepec&#59; el movimiento absoluto de la placa de Am&#233;rica del Norte&#59; y el hundimiento de la litosfera debido a la acumulaci&#243;n de la carga de los sedimentos&#46;</p><p id="spar0015" class="elsevierStyleSimplePara elsevierViewall">Usamos los registros del sismo de 1997 como funci&#243;n de Green emp&#237;rica para simular los movimientos de tierra en la regi&#243;n epicentral de un sismo de <span class="elsevierStyleItalic">M</span><span class="elsevierStyleInf">w</span>6&#46;4 postulado en la cuenca Comalcalco&#46; Bajo supuestos razonables&#44; los valores esperados de aceleraci&#243;n&#44; velocidad y desplazamiento picos son 120-260 gales&#44; 12 a 28<span class="elsevierStyleHsp" style=""></span>cm&#47;s&#44; y 6 a 11<span class="elsevierStyleHsp" style=""></span>cm&#44; respectivamente&#46; La extensa licuefacci&#243;n reportada en Coatzacoalcos durante el sismo de 1959&#44; <span class="elsevierStyleItalic">M</span><span class="elsevierStyleInf">w</span>6&#46;4&#44; sugiere que los sedimentos de la cuenca se comportan de manera no lineal bajo tal excitaci&#243;n&#46;</p></span>"
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      "en" => array:2 [
        "titulo" => "Abstract"
        "resumen" => "<span id="abst0010" class="elsevierStyleSection elsevierViewall"><p id="spar0020" class="elsevierStyleSimplePara elsevierViewall">We analyze the 6 September 1997<span class="elsevierStyleHsp" style=""></span><span class="elsevierStyleItalic">M</span><span class="elsevierStyleInf">w</span>4&#46;5 earthquake&#44; which occurred about 25<span class="elsevierStyleHsp" style=""></span>km SE of Coatzacoalcos&#44; Veracruz&#46; The earthquake was recorded by the local broadband station TUIG &#40;S-P time &#61; 5 s&#41;&#46; P-wave polarities at regional and teleseismic distances and modeling of the displacement waveforms at TUIG yields a thrust-faulting focal mechanism &#40;f &#61; 150&#176;&#59; d &#61; 70&#176;&#59; l &#61; 90&#176;&#41;&#46; In the same region a destructive <span class="elsevierStyleItalic">M</span><span class="elsevierStyleInf">w</span>6&#46;4 earthquake occurred on 26 August 1959 at a similar depth and with a similar mechanism&#46; The analysis of the 1997 event reinforces a previous conclusion that the lower crust beneath the Comalcalco basin is in a thrust-faulting stress regime&#44; in contrast to the shallow part of the crust&#44; which is characterized by normal-faulting&#59; this implies a permutation with depth of the maximum and minimum principal stresses&#46; It agrees with observations elsewhere that the state of stress in sedimentary basins can be different from the one at greater depth&#46;</p><p id="spar0025" class="elsevierStyleSimplePara elsevierViewall">Focal mechanisms are available for seven earthquakes in and near the Gulf of Mexico&#46; All of these events indicate a thrust-faulting type stress regime at mid- and lower-crustal levels&#46; The observed trend of the P axes of these earthquakes can be explained by one or more of the following causes&#58; strong coupling along the subduction plate interface offshore Tehuantepec&#59; absolute motion of the North American plate&#59; and downwarping of the lithosphere due to sediment loading&#46;</p><p id="spar0030" class="elsevierStyleSimplePara elsevierViewall">By using the recordings of the 1997 event as empirical Green&#39;s function&#44; we simulate the ground motions in the epicentral region of a postulated <span class="elsevierStyleItalic">M</span><span class="elsevierStyleInf">w</span>6&#46;4 earthquake in the Comalcalco basin&#46; Under reasonable assumptions&#44; the expected peak acceletion&#44; velocity and displacement are 120-260<span class="elsevierStyleHsp" style=""></span>gal&#44; 12-28<span class="elsevierStyleHsp" style=""></span>cm&#47;s&#44; and 6-11<span class="elsevierStyleHsp" style=""></span>cm&#44; respectively&#46; The extensive soil liquefaction in Coatzacoalcos during the 1959&#44; <span class="elsevierStyleItalic">M</span><span class="elsevierStyleInf">w</span>6&#46;4&#44; earthquake suggests that the sediments of the basin behave nonlinearly under such excitation&#46;</p></span>"
      ]
    ]
    "multimedia" => array:11 [
      0 => array:7 [
        "identificador" => "fig0005"
        "etiqueta" => "Figure 1"
        "tipo" => "MULTIMEDIAFIGURA"
        "mostrarFloat" => true
        "mostrarDisplay" => false
        "figura" => array:1 [
          0 => array:4 [
            "imagen" => "gr1.jpeg"
            "Alto" => 1096
            "Ancho" => 1183
            "Tamanyo" => 233097
          ]
        ]
        "descripcion" => array:1 [
          "en" => "<p id="spar0035" class="elsevierStyleSimplePara elsevierViewall">Earthquakes in and near Gulf of Mexico with known focal mechanism&#46; Source parameters of the events are listed in <a class="elsevierStyleCrossRef" href="#tbl0010">Table 2</a>&#46; Focal mechanisms show that the mid- and lower crust of the Gulf is under compressive stress regime&#46; Dotted lines indicate the bathymetry of the Gulf and gray dashed lines denote the limits of the buried salt deposits&#46; LVPP &#61; Laguna Verde Power Plant&#46; Triangle shows location of station TUIG&#46;</p>"
        ]
      ]
      1 => array:7 [
        "identificador" => "fig0010"
        "etiqueta" => "Figure 2"
        "tipo" => "MULTIMEDIAFIGURA"
        "mostrarFloat" => true
        "mostrarDisplay" => false
        "figura" => array:1 [
          0 => array:4 [
            "imagen" => "gr2.jpeg"
            "Alto" => 573
            "Ancho" => 1872
            "Tamanyo" => 132680
          ]
        ]
        "descripcion" => array:1 [
          "en" => "<p id="spar0040" class="elsevierStyleSimplePara elsevierViewall">Seismograms at station TUIG during the 6 September 1997 earthquake&#46; &#40;a&#41; Acceleration&#44; &#40;b&#41; velocity&#44; and &#40;c&#41; displacement&#46; The traces in &#40;b&#41; and &#40;c&#41; have been obtained by integration of the accelerograms shown in &#40;a&#41;&#46;</p>"
        ]
      ]
      2 => array:7 [
        "identificador" => "fig0015"
        "etiqueta" => "Figure 3"
        "tipo" => "MULTIMEDIAFIGURA"
        "mostrarFloat" => true
        "mostrarDisplay" => false
        "figura" => array:1 [
          0 => array:4 [
            "imagen" => "gr3.jpeg"
            "Alto" => 877
            "Ancho" => 882
            "Tamanyo" => 88986
          ]
        ]
        "descripcion" => array:1 [
          "en" => "<p id="spar0045" class="elsevierStyleSimplePara elsevierViewall">Initial part of the three components of displacement at TUIG&#46; The horizontal components have been multiplied by 20&#46;</p>"
        ]
      ]
      3 => array:7 [
        "identificador" => "fig0020"
        "etiqueta" => "Figure 4"
        "tipo" => "MULTIMEDIAFIGURA"
        "mostrarFloat" => true
        "mostrarDisplay" => false
        "figura" => array:1 [
          0 => array:4 [
            "imagen" => "gr4.jpeg"
            "Alto" => 1313
            "Ancho" => 1351
            "Tamanyo" => 189743
          ]
        ]
        "descripcion" => array:1 [
          "en" => "<p id="spar0050" class="elsevierStyleSimplePara elsevierViewall">&#40;Top&#41; <span class="elsevierStyleItalic">P</span>-wave first motions of the 1997 earthquake plotted on lower-hemisphere&#44; equal-area projection&#46; With the exception of TUIG&#44; all Mexican broadband stations recorded dilatation &#40;open circles&#41;&#46; Three teleseismic stations and TUIG show compression &#40;solid circles&#41;&#46; Focal mechanism&#44; f &#61; 150&#176;&#59; d &#61; 70&#176;&#59; l &#61; 90&#176;&#44; which satisfies first-motion data&#44; and the waveform at TUIG is shown&#46; &#40;Bottom&#44; left&#41; Comparison of observed and infinite-space synthetic seismograms at station TUIG&#46; &#40;Bottom&#44; right&#41; Comparison of observed and synthetic seismograms at station TUIG&#46; Synthetics were computed using crustal model and focal parameters given in <a class="elsevierStyleCrossRefs" href="#tbl0005">Tables 1 and 2</a>&#44; respectively&#46;</p>"
        ]
      ]
      4 => array:7 [
        "identificador" => "fig0025"
        "etiqueta" => "Figure 5"
        "tipo" => "MULTIMEDIAFIGURA"
        "mostrarFloat" => true
        "mostrarDisplay" => false
        "figura" => array:1 [
          0 => array:4 [
            "imagen" => "gr5.jpeg"
            "Alto" => 588
            "Ancho" => 1869
            "Tamanyo" => 148314
          ]
        ]
        "descripcion" => array:1 [
          "en" => "<p id="spar0055" class="elsevierStyleSimplePara elsevierViewall">An example of simulated acceleration&#44; velocity&#44; and displacement traces in the epicentral region from a postulated <span class="elsevierStyleItalic">M</span><span class="elsevierStyleInf">w</span>6&#46;5 earthquake&#44; using recording of the 1997 earthquake as empirical Green&#39;s function &#40;stress drop of EGF &#61; stress drop of target earthquake &#61; 6<span class="elsevierStyleHsp" style=""></span>MPa&#41;&#46; The right frame also shows&#44; by dashed lines&#44; the deterministic&#44; synthetic displacement seismograms at TUIG for an <span class="elsevierStyleItalic">M</span><span class="elsevierStyleInf">w</span>6&#46;5 earthquake located at the focus of the 1997 event&#46;</p>"
        ]
      ]
      5 => array:7 [
        "identificador" => "tbl0005"
        "etiqueta" => "Table 1"
        "tipo" => "MULTIMEDIATABLA"
        "mostrarFloat" => true
        "mostrarDisplay" => false
        "tabla" => array:1 [
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                  <table border="0" frame="\n
                  \t\t\t\t\tvoid\n
                  \t\t\t\t" class=""><thead title="thead"><tr title="table-row"><th class="td" title="table-head  " align="left" valign="top" scope="col" style="border-bottom: 2px solid black">Layer&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</th><th class="td" title="table-head  " align="left" valign="top" scope="col" style="border-bottom: 2px solid black">Thickness km&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</th><th class="td" title="table-head  " align="left" valign="top" scope="col" style="border-bottom: 2px solid black">P-wave speed <span class="elsevierStyleItalic">&#945;</span>&#44; km&#47;s&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</th><th class="td" title="table-head  " align="left" valign="top" scope="col" style="border-bottom: 2px solid black">S-wave speed &#946;&#44; km&#47;s&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</th><th class="td" title="table-head  " align="left" valign="top" scope="col" style="border-bottom: 2px solid black">Density gm&#47;cm<span class="elsevierStyleSup">3</span>&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</th><th class="td" title="table-head  " align="left" valign="top" scope="col" style="border-bottom: 2px solid black">Quality <span class="elsevierStyleItalic">Q</span><span class="elsevierStyleInf">a</span>&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</th><th class="td" title="table-head  " align="left" valign="top" scope="col" style="border-bottom: 2px solid black">Factor <span class="elsevierStyleItalic">Q</span><span class="elsevierStyleInf">&#946;</span>&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</th></tr></thead><tbody title="tbody"><tr title="table-row"><td class="td-with-role" title="table-entry ; entry_with_role_rowhead " align="left" valign="top">1&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="left" valign="top">1&#46;8&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="left" valign="top">2&#46;80&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="left" valign="top">1&#46;40&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="left" valign="top">2&#46;70&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="left" valign="top">80&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="left" valign="top">40&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td></tr><tr title="table-row"><td class="td-with-role" title="table-entry ; entry_with_role_rowhead " align="left" valign="top">2&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="left" valign="top">15&#46;6&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="left" valign="top">4&#46;25&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="left" valign="top">2&#46;40&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="left" valign="top">2&#46;80&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="left" valign="top">300&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="left" valign="top">200&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td></tr><tr title="table-row"><td class="td-with-role" title="table-entry ; entry_with_role_rowhead " align="left" valign="top">3&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="left" valign="top">&#8734;&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="left" valign="top">6&#46;50&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="left" valign="top">3&#46;75&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="left" valign="top">2&#46;85&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="left" valign="top">400&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="left" valign="top">300&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td></tr></tbody></table>
                  """
              ]
              "imagenFichero" => array:1 [
                0 => "xTab890459.png"
              ]
            ]
          ]
        ]
        "descripcion" => array:1 [
          "en" => "<p id="spar0060" class="elsevierStyleSimplePara elsevierViewall">Crustal model near Coatzacoalcos used in the synthesis of ground motion&#46;</p>"
        ]
      ]
      6 => array:7 [
        "identificador" => "tbl0010"
        "etiqueta" => "Table 2"
        "tipo" => "MULTIMEDIATABLA"
        "mostrarFloat" => true
        "mostrarDisplay" => false
        "tabla" => array:2 [
          "leyenda" => "<p id="spar0070" class="elsevierStyleSimplePara elsevierViewall"><span class="elsevierStyleSup">a</span> Location from International Seismological Summary&#44; ISS&#59; depth&#44; focal mechanism&#44; and <span class="elsevierStyleItalic">M</span><span class="elsevierStyleInf">w</span> from <a class="elsevierStyleCrossRef" href="#bib0125">Su&#225;rez &#40;2000&#41;</a>&#46;</p><p id="spar0075" class="elsevierStyleSimplePara elsevierViewall"><span class="elsevierStyleSup">b</span> Location from International Seismological Centre&#44; ISC&#59; depth&#44; focal mechanism&#44; and <span class="elsevierStyleItalic">M</span><span class="elsevierStyleInf">w</span> from <a class="elsevierStyleCrossRef" href="#bib0125">Su&#225;rez &#40;2000&#41;</a>&#46;</p><p id="spar0080" class="elsevierStyleSimplePara elsevierViewall"><span class="elsevierStyleSup">c</span> Location&#44; depth&#44; and focal mechanism from <a class="elsevierStyleCrossRef" href="#bib0050">Frohlich &#40;1982&#41;</a>&#46; The two mechanisms are extreme types consistent with first-motion data&#46;</p><p id="spar0085" class="elsevierStyleSimplePara elsevierViewall"><span class="elsevierStyleSup">d</span> This study&#46;</p><p id="spar0090" class="elsevierStyleSimplePara elsevierViewall"><span class="elsevierStyleSup">e</span> Global Centroid Moment Tensor &#40;CMT&#41; catalog&#46;</p><p id="spar0095" class="elsevierStyleSimplePara elsevierViewall"><span class="elsevierStyleSup">f</span> Source parameters listed in <span class="elsevierStyleInterRef" id="intr0005" href="http://www.eas.slu.edu/eqc/eqc_mt/MECH.NA/20070523190916/index.html">http&#58;&#47;&#47;www&#46;eas&#46;slu&#46;edu&#47;eqc&#47;eqc&#95;mt&#47;MECH&#46;NA&#47;20070523190916&#47;index&#46;html</span></p><p id="spar0100" class="elsevierStyleSimplePara elsevierViewall"><span class="elsevierStyleSup">g</span><a class="elsevierStyleCrossRef" href="#bib0045">Franco <span class="elsevierStyleItalic">et al</span>&#46; &#40;2013&#41;</a></p>"
          "tablatextoimagen" => array:1 [
            0 => array:2 [
              "tabla" => array:1 [
                0 => """
                  <table border="0" frame="\n
                  \t\t\t\t\tvoid\n
                  \t\t\t\t" class=""><thead title="thead"><tr title="table-row"><th class="td" title="table-head  " align="left" valign="top" scope="col" style="border-bottom: 2px solid black">No&#46;&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</th><th class="td" title="table-head  " align="left" valign="top" scope="col" style="border-bottom: 2px solid black">Date&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</th><th class="td" title="table-head  " align="left" valign="top" scope="col" style="border-bottom: 2px solid black">Latitude &#176;N&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</th><th class="td" title="table-head  " align="left" valign="top" scope="col" style="border-bottom: 2px solid black">Longitude &#176;W&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</th><th class="td" title="table-head  " align="left" valign="top" scope="col" style="border-bottom: 2px solid black">Depth km&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</th><th class="td" title="table-head  " align="left" valign="top" scope="col" style="border-bottom: 2px solid black"><span class="elsevierStyleItalic">M</span><span class="elsevierStyleInf">w</span>&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</th><th class="td" title="table-head  " align="left" valign="top" scope="col" style="border-bottom: 2px solid black">Focal Mechanism &#981;&#8217;&#176;&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</th><th class="td" title="table-head  " align="left" valign="top" scope="col" style="border-bottom: 2px solid black">&#948;&#8217;&#176;&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</th><th class="td" title="table-head  " align="left" valign="top" scope="col" style="border-bottom: 2px solid black">&#955;&#8217;&#176;&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</th></tr></thead><tbody title="tbody"><tr title="table-row"><td class="td-with-role" title="table-entry ; entry_with_role_rowhead " align="left" valign="top">1<span class="elsevierStyleSup">a</span>&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="left" valign="top">26 Aug 1959&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="left" valign="top">18&#46;26&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="left" valign="top">94&#46;43&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="left" valign="top">21&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="left" valign="top">6&#46;4&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="left" valign="top">309&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="left" valign="top">32&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="left" valign="top">102&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td></tr><tr title="table-row"><td class="td-with-role" title="table-entry ; entry_with_role_rowhead " align="left" valign="top">2<span class="elsevierStyleSup">b</span>&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="left" valign="top">11 Mar 1967&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="left" valign="top">19&#46;23&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="left" valign="top">95&#46;74&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="left" valign="top">26&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="left" valign="top">5&#46;7&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="left" valign="top">250&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="left" valign="top">39&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="left" valign="top">20&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td></tr><tr title="table-row"><td class="td-with-role" title="table-entry ; entry_with_role_rowhead " align="left" valign="top">3<span class="elsevierStyleSup">c</span>&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="left" valign="top">24 Jul 1978&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="left" valign="top">26&#46;49&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="left" valign="top">88&#46;79&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="left" valign="top">15&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="left" valign="top">5&#46;0&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="left" valign="top">225&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="left" valign="top">49&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="left" valign="top">111&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td></tr><tr title="table-row"><td class="td" title="table-entry  " align="" valign="top">&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="" valign="top">&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="" valign="top">&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="" valign="top">&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="" valign="top">&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="" valign="top">&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="left" valign="top">240&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="left" valign="top">63&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="left" valign="top">52&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td></tr><tr title="table-row"><td class="td-with-role" title="table-entry ; entry_with_role_rowhead " align="left" valign="top">4<span class="elsevierStyleSup">d</span>&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="left" valign="top">06 Sep 1997&nbsp;\t\t\t\t\t\t\n
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                "etiqueta" => "Zoback&#44; 1990"
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                    "referenciaCompleta" => "Zoback M&#46;L&#46; &#44; <span class="elsevierStyleItalic">et al</span>&#46;&#44; 1990&#44; Stress map of North America&#44; Geological Society of America&#44; The Decade of North American Geology&#44; Continent-scale map- 005&#44; 1&#58;5&#44;000&#44;000&#46;"
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        "titulo" => "Acknowledgments"
        "texto" => "<p id="par0125" class="elsevierStylePara elsevierViewall">We benefited from discussions with Antonio Camargo and Daniel Res&#233;ndiz&#46; Bruce Presgrave kindly provided us with teleseismic first-motion readings of the earthquake&#46; We thank an anonymous reviewer for his comments which significantly improved the manuscript&#46; The research was partially funded by DGAPA&#44; UNAM &#40;IN111314&#41;&#46;</p>"
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Article information

ISSN: 00167169
Original language: English

DOI:10.1016/j.gi.2015.08.001

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Year/Month	Html	Pdf	Total

2024 November	2	0	2
2024 October	25	3	28
2024 September	39	2	41
2024 August	39	4	43
2024 July	14	1	15
2024 June	28	3	31
2024 May	34	2	36
2024 April	19	8	27
2024 March	29	5	34
2024 February	12	2	14
2024 January	18	6	24
2023 December	12	10	22
2023 November	16	2	18
2023 October	23	10	33
2023 September	21	3	24
2023 August	14	3	17
2023 July	22	12	34
2023 June	11	5	16
2023 May	19	4	23
2023 April	11	1	12
2023 March	25	2	27
2023 February	30	7	37
2023 January	17	7	24
2022 December	26	2	28
2022 November	23	8	31
2022 October	30	9	39
2022 September	22	10	32
2022 August	13	12	25
2022 July	14	9	23
2022 June	18	6	24
2022 May	32	7	39
2022 April	15	11	26
2022 March	23	9	32
2022 February	16	7	23
2022 January	27	7	34
2021 December	13	11	24
2021 November	24	14	38
2021 October	25	12	37
2021 September	20	10	30
2021 August	22	6	28
2021 July	21	9	30
2021 June	120	8	128
2021 May	14	7	21
2021 April	24	23	47
2021 March	15	50	65
2021 February	7	20	27
2021 January	18	10	28
2020 December	28	10	38
2020 November	22	10	32
2020 October	46	5	51
2020 September	13	14	27
2020 August	14	10	24
2020 July	11	9	20
2020 June	10	3	13
2020 May	15	10	25
2020 April	9	1	10
2020 March	13	10	23
2020 February	14	3	17
2020 January	15	8	23
2019 December	18	6	24
2019 November	15	9	24
2019 October	17	8	25
2019 September	16	13	29
2019 August	11	11	22
2019 July	21	13	34
2019 June	53	34	87
2019 May	113	81	194
2019 April	67	37	104
2019 March	19	7	26
2019 February	27	5	32
2019 January	10	3	13
2018 December	15	3	18
2018 November	16	6	22
2018 October	35	8	43
2018 September	23	11	34
2018 August	25	11	36
2018 July	16	9	25
2018 June	22	6	28
2018 May	27	12	39
2018 April	24	7	31
2018 March	16	2	18
2018 February	21	5	26
2018 January	20	6	26
2017 December	18	4	22
2017 November	32	4	36
2017 October	22	4	26
2017 September	17	12	29
2017 August	26	7	33
2017 July	25	5	30
2017 June	43	24	67
2017 May	27	7	34
2017 April	17	26	43
2017 March	19	77	96
2017 February	28	4	32
2017 January	18	2	20
2016 December	33	17	50
2016 November	36	10	46
2016 October	30	15	45
2016 September	28	6	34
2016 August	21	3	24
2016 July	26	3	29
2016 June	18	18	36
2016 May	14	20	34
2016 April	19	19	38
2016 March	19	23	42
2016 February	20	14	34
2016 January	15	15	30
2015 December	19	18	37
2015 November	16	16	32
2015 October	20	19	39
2015 September	10	8	18

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